Water-Supply and Irrigation Paper No* 167 

G B 

102>5 

UsRs 



benes I Q^ Underground Waters, 



63 



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DEPARTMEiMi Ub THE INTEKiOR 

ITED STATES GEOLOGICAL SURVEY 

CHARLES D. WALCOTT, Director 



UNDERGROUND WATER 



IN THE 



VALLEYS OF UTAH LAKE AND JORDAN RIYER, OTAH 



BY 



G. B. RICHARDSON 




WASHINGTON 

GOVERNMENT PRINTING OFFICE 
1906 




Pass G[l ^l02.S 
Book U ^1^5 



f f 



Water-Supply and Irrigation Paper No. 157 



S«ri«<; i ^' Descriptive Geology, 86 
^®^^®^ \ 0, Underground Waters, 53 



DEPARTMENT OF THE INTERIOR 
UNITED STATES GEOLOGICAL SURVEY 

CHARLES I). WALCOTT, Director 



y^y- 



UNDERGROUND WATER 



IN THE 



VALLEYS OF UTAH LAKE AND JORDAN RIVER, UTAH 



BY 



G. B. RICHARDSON 




WASHINGTON 

GOVERNMENT P R I N T I N (i C) F I<' I C E 
19 06 



VjX 



CONTENTS 



Page. 

Introduction 5 

Topography and drainage 5 

Geology 7 

Literature 7 

Descriptive geology of the highlands 8 

Late geologic history 11 

Tertiary 11 

Quaternary 11 

Climate 13 

Precipitation 14 

Temperature 15 

Wind velocity 16 

Humidity 16 

Evaporation 17 

Summary 17 

Hydrography : 18 

Streams tributary to Utah Lake and Jordan River 18 

Utah Lake 23 

Jordan River 24 

Great Salt Lake 25 

Underground water 27 

General conditions 27 

Source 27 

Distribution 29 

Quality 30 

Recovery 35 

Suggestions 38 

Occurrence 38 

West of Jordan River 38 

Divisions of area 38 

Upland area 39 

Lowland area 41 

East of Jordan River 43 

Salt Lake City 43 

South of Salt Lake City i 45 

Utah Lake Valley 48 

Lehi and vicinity 48 

American Fork, Pleasant Grove, and vicinity 49 

Provo and vicinity 51 

Springville and vicinity 52 

Spanish Fork, Payson, and vicinity 53 

Goshen Valley ■'yn 

West of Utah Lake 56 

3 



4 CONTENTS AND ILLUSTRATIONS. 

Underground water — Continued. Page. 

Well data 56 

Method of measurement 56 

List of typical wells 59 

Index 77 



ILLUSTRATIONS. 



[Yate I. Wasatch Mountains from Liberty Park, Salt Lake City 5 

IL Map of the valleys of Utah Lake and Jordan River, showing drainage 

area 6 

III; A, Northern end of Utah Lake; B, Head-gate of Jordan and Salt Lake 

City canal 12 

IV. A, Gate at head of Jordan River; B, Dead Man's Falls, Cottonwood 

Canyon. 24 

V.'- Well sections 28 

VI. Sketch map showing depth to ground water in the valleys of Utah Lake 

and Jordan River 30 

VII.' Map showing the area in which flowing wells are obtained in Jordan 

River Valley 38 

VIIL= Map showing the area in which flowing wells are obtained in Utah Lake 

Valley. 48 

IX. A, Valley of Provo River below mouth of canyon; B, American Fork 

at mouth of canyon. 50 

Fig. 1. Diagram showing variation of annual precipitation at Salt Lake City 17 

2. Diagram showing mean monthly precipitation at Salt Lake City 18 

3. Diagram showing fluctuation of the surface of Utah Lake, 1889-1904 23 

4. Diagram showing fluctuation of the surface of Great Salt Lake, 1873-1903. . . 26 

5. Diagram illustrating flow from vertical and horizontal pipes ^ 57 




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o 



UNDERGROUND WATER IN THE VALLEYS OF UTAH 
LAKE AND JORDAN RIVER, UTAH. 



By G. B. Ric;hardson. 



INTRODUCTION. 

The valleys of Utah Lake and Jordan River are situated in north-central Utah, in the 
extreme eastern part of the Great Basin. The lofty Wasatch Range (PI. I), the western- 
most of the Rocky Mountain system, limits the valleys on the east, and relatively low- 
basin ranges — the Oquirrh, Lake, and East Tintic mountains — determine them on the 
west. The valleys trend north and south, and are almost separated by the low east- west 
Traverse Range, the slopes of which constitute a dam for Utah Lake, which drains through 
Jordan River to Great Salt Lake. 

The area under consideration is the most populous and flourishing part of the State. 
Salt Lake City and Provo, the first and tliird cities in the State, and many other thriving 
settlements are there located. At Bingham Junction and Murray a number of smelters 
treat the ores from near-by mines, but agriculture is the main industry. Water for irriga- 
tion is supplied by mountain streams, and intensive farming is successfully pursued. 
The practice of irrigation was begun by the Mormon pioneers in 1847, and has been dis- 
cussed in several publications; little attention, however, has been given to the under- 
ground water resources, and, so far as the writer is aware, they have not before been 
described. The present paper outlines conditions of occurrence of the subterranean 
waters and describes their development in the valleys of Utah Lake and Jordan River. 

TOPOGRAPHY AND DRAINAGE. 

The drainage area of Utah Lake and Jordan River is approximately 3,300 square miles, 
of which 2,600 are tributary to Utah Lake and 700 to the Jordan north of the Traverse 
Mountains (PI, II). About 2,000 square miles of the watershed are in the Wasatch 
Mountains, while the valleys themselves cover a little less than 1,000 square miles. Utah 
Lake Valley is about 38 miles long, averages 15 miles in width, and occupies about 560 
square miles, including Utah Lake. Jordan Valley is approximately 28 miles long, 15 
miles wide, and comprises 420 square miles. These valleys in late geologic time aw re 
occupied by Lake Bonneville, the Pleistocene predecessor of Great Salt Lake, and to 
that fact is due their characteristic topography. Almost flat unconsolidated lake sedi- 
ments underlie the broad valleys, the borders of which are marked by a unique series 
of terraces that characterize the shore lines of the old lake. Descriptive details of these 
features will be given in the sections devoted to geology and to the occurrence of under- 
ground water. 

The range in elevation is considerable. The present level of Great Salt Lake is approxi- 
mately 4,210 feet above the sea, and that of Utah Lake is about 4,480 feet. From these 
lowest elevations the two valleys rise to their outer borders, which may conveniently be 
taken as the highest level occupied by Lake Bonneville, at approximately the 5,200-foot 
contour, above which the Wasatch Range towers up to 12,000 feet. The mountains on 
the west are narrow north-south ranges that rise abruptly from broad valleys. The 



b UNDERGROUND WATER IN VALLEYS OF UTAH. 

Oquirrh Mountains, west of Jordan River, are 30 miles long, 5 to 10 miles wide, and their 
summits rise to elevations of about 10,000 feet. The Lake Mountains, west of Utah 
Lake, are about 15 miles long, 5 miles wide, and 3,000 feet above the lake. They are 
connected by low hills with the Oquirrh Mountains on the north and with the East Tintic 
Mountains on the south.- The East Tintic Mountains border Utah Lake Valley on the 
southwest, rising above it about 3,000 feet. A spur from these mountains extends north- 
eastward, constituting the southern border of Utah Lake Valley, and almost unites with 
the Wasatch Range. The steep western face of the Wasatch Mountains rises about 7,000 
feet abruptly above the broad valley and constitutes the dominant topographic feature 
of the region. To the east the range slopes away gradually in a series of broad ridges 
and narrow valleys to the mountainous plateau region. The western scarp is deeply 
dissected by canyons, through which the entire Wasatch drainage flows to Great Salt 
Lake, the chief streams being Bear, Weber, and Jordan rivers. 

Utah Lake is a body of shallow water about 21 miles long and 7 miles wide (PI. Ill, A), 
covering a maximum area of 93,000 acres. Its depth over much of its extent is only 8 
feet or less, and the maximum depth in the main body of the lake is about 13 feet. In 
its northwestern part, however, recent soundings have revealed the presence of several 
deep holes, due to springs (p. 49). The shore line of the lake is subject to considerable 
variation, owing to the changing relations of evaporation, precipitation, and inflow, and 
the margins are characteristically swampy. Two large, shallow bays extend eastward 
and southward from the main body of the lake, one south of Provo and the other north 
of Goshen. West of the lake the Pelican Hills approach close to the shore, and the region 
is barren, but on the north, east, and south the land rises gently toward the base of the 
mountains and is dotted with flourishing settlements which are supported by irrigation. 

The principal streams tributary to Utah Lake, beginning at the north and proceeding 
southward, are: Dry, American Fork, Battle, and Grove creeks, Provo River, Hobble 
Creek, Spanish Fork, and Peteeneet, Santaquin, and Currant creeks. Of these, Provo 
River is the largest, being approximately 70 miles long and having a drainage area of 640 
square miles. It rises in the Uinta Mountains near the sources of Weber, Bear, and 
Du Chesne rivers, flows westward and southward through Kam.as and Provo valleys, and 
passes through the Wasatch Mountains in a deep canyon. On entering Utah Lake Valley 
Provo River flows almost due south for 5 miles, skirting the great Provo delta, and thence 
westward, entering Utah Lake about 3 miles west of Provo. 

Spanish Fork has a watershed about equal to that of Provo River, but not so great 
a discharge. It rises near Soldier Summit, and, after receiving two main tributaries. 
North and Thistle creeks, flows in a canyon through the main ridge of the Wasatch Moun- 
tains and enters Utah Lake Valley at the head of the large embayment that extends between 
Payson and Springville, 

Salt Creek rises in the southern Wasatch Mountains, on the eastern slope of Mount Nebo, 
and, after crossing the border of the plateau region, emerges into the broad valley at the 
southwestern base of the Wasatch Mountains where, in summer, it ceases to flow at the 
surface. The drainage way continues, in a narrow canyon, through Long Ridge which par- 
tially connects the East Tintic and the Wasatch mountains, and enters the southern end 
of Utah Lake in Goshen Valley, where the stream, which is fed largely by seepage, is known 
as Currant Creek. 

The other tributaries of Utah Lake are relatively small. The chief ones rise in the 
Wasatch Mountains and occupy canyons in their mountain courses, where they maintain 
perennial flows. At the mouths of the canyons canals divert the water and distribute it 
over the valley, so that in the irrigation season practically all of the available supply is 
thus used and the beds of the streams in Utah Lake Valley are commonly dry; but in the 
late spring and early summer, during the period of melting snow, large volumes are dis- 
charged directly into the lake. 

Jordan River heads at the northern end of Utah Lake and flows northward in a meander- 
ing course of about 40 miles to Great Salt Lake. For the first 5 miles the river flows slug- 








--^•^^sik*. 










l]L^^^'^y 



TOPOGRAPHY AND DRAINAGE. Y 

gishly in a broad valley, and in that distance falls only about 10 foot. In tho "narrows," 
however, the river occupies a constricted channel and descends rapidly; in the first mile 
below the intake of the canals its fall amounts to about 70 f(ct. Below the ''narrows" the 
valley spreads out and at its greatest width is about 18 miles wide. The country rises gradu- 
ally toward the adjacent highlands to the base of the terraces that mark the shore lines of 
Lake Bonneville, whence tho ascent is by successive steps. Between Salt Lake City and 
Great Salt Lake the topography is almost flat, and a numl)er of small lakes of shifting out- 
line occupy local depressions. As the shore of Great Salt Lake is approached there is a 
faint slope of the surface which becomes increasingly marshy. This area west of Salt Lake 
City in general is barren and desolate and the surface in many places is white with alkali. 
On the uplands, away from the lake, alkali is scarce, but the western part of the valley, 
because of the lack of water, suffers in comparison with the cultivated eastern part, which 
is supplied by streams from the Wasatch Mountains. 

North of the Traverse Mountains the principal tributaries of Jordan River are City, Red 
Butte, Emigration, Parleys, Mill, Big Cottonwood, Little Cottonwood, Dry Cottonwood, and 
Willow creeks, all of which issue from the Wasatch. In their mountain courses these creeks 
generally occupy narrow canyons from which they emerge on the lowlands and flow in broad 
open valleys to the Jordan. Within the mountains they are all perennial streams, but at 
the mouths of the canyons their flow is largely diverted by irrigation ditches, so that, in the 
dryest part of the year, their lower courses are generally dry. They rise in the main crest 
of the Wasatch and have small watersheds. Big Cottonwood Creek, draining about 48 square 
miles, being the largest. This stream rises at the base of Clayton Peak, is fed by a number 
of small lakes, and discharges a considerable quantity of water through a narrow canyon 
(PI. IV, 5). 

The vegetation is scanty. The valleys in their natural state are occupied by sagebrush, 
greasewood, and kindred desert plants, but wherever water is available there is a marked 
contrast, and the irrigated areas of these valleys rival in productiveness an}^ in the country. 
Sugar beets are grown in quantity; alfalfa, potatoes, corn, etc., are common crops; and on 
the bench lands a variety of fruits are successfully cultivated. The mountains on the 
western border are generally barren; sagebrush and occasional cacti are the chief growths 
on the slopes, while scrub oak and stunted spruce and pine here and there grow in 
patches; the summits are usually bare. The Wasatch Mountains are more favored, but 
they do not support a heavy growth of trees. At the heads of the valleys scattering 
pine, juniper, mountain mahogany, and quaking aspen locally occur, and cottonwood, birch, 
and maple are often found near the stream beds. The slopes are commonly covered with 
underbrush in varying degrees of thickness, sagebrush and scrub oak being prominent. 

GEOLOGY. 

LITERATURE. 

This area has been studied by prominent geologists and has inspired some classic works 
on American geology. King, Emmons, and Hague of the Fortieth Parallel Survey « inter- 
preted the main features of the region, and Gilbert made it famous by his investigation of 
Lake Bonneville. t But although this interesting region lies contiguous to one of tho main 
transcontinental routes and has been visited by many geologists, yet comparatively little 
detailed work has been done in it. Walcottc has studied tho Big Cottonwood Cambrian 
section, G. O. Smith and G. W. Tower rf have examined the Tintic district, J. E. Spurrf has 

a King, Clarence, Systematic geology: Rept. Geol. Explor. 40th Par,, vol. 1, 1872; Hague, Arnold, and 
Emmons, S. F., Descriptive geology: Ibid., vol. 2, 1877. 

b Gilbert, G. K., Lake Bonneville: Mon. U. S. Geol. Survey, vol. 1, 1890. 

cWalcott, C. D., Bull. U. S. Geol. Survey Nc. 30, 1880, p. 38. 

d Tower, G. W., and Smith, G. O., Geology and mining industry of the Tintic district, Utah: Nine- 
teenth Ann. Rept. U. S. Geol. Survey, pt. 3, 1898, p. m\. 

<Spurr,.J. E., Economic geology of the Mercur mining district, Utah. Sixteenth Ann. Kept. U. S. 
Geol. Survey, pt. 2, 1895, p. 343. 



8 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



reported on the Mercur mines, and, more recently, work has been carried on in the Park 
City and Bingham mining districts by J. M. Boutwell.a The following sketch is mainly 
compiled from these reports. 

DESCRIPTIVE GEOLOGY OF THE HIGHLA^^DS. 

The Wasatch Mountains are composed of a complex mass of sedimentary, igneous, and 
metamorphic rocks that have been much folded and faulted. In age the rocks range from 
pre-Cambrian to Tertiary and constitute a thickness of about 50,000 feet. The following 
table shows in epitome the main Paleozoic divisions according to the Fortieth Parallel 
Survey: 

Paleozoic section in the Wasatch Mountains. 



System. 


Formation. 


Average 
thickness. 




["Upper Carboniferous limestone (including Permian) 


Feet. 
2, 500 to 3, 000 
5, 000 to 7, 000 
7,000 
1,000 to 1,250 
1,000 to 1,250 
12,000 


Carboniferous 


< Weber quartzites with a few thin beds of limestone. 




[ Wasatch limestone 


Devonian 


Ogden quartzite 


Silurian 






Big Cottonwood quartzite series (clay slates at top) 








30,000 



The present mountains are the eastern part of a greater mass of rocks, the Wasatch 
Range having been raised by faulting several thousand feet higher than the western part 
of this mass, which now lies buried beneath the valley deposits. This great fault is the 
dominant structural feature of the region. The range rises abruptly 7,000 feet above the 
wide lowland at its base, where the streams,,which in their mountain courses occupy deep- 
cut narrow gorges, flow in wide valleys. The fault cuts across the range regardless of the 
structure of the rocks, and the truncated mountain bases abut against the plain in marked 
alignment. 

Beginning at the north and proceeding southward the following features may be noted: 
The spur that juts out from the Wasatch Mountains north of Salt Lake City marks the 
southern boundary of a series of pre-Cambrian rocks that constitute the crest and western 
flanks of the mountains to the northwest, almost as far as Ogden. These rocks for the 
most part consist of gneisses and mica-schists, considered to be of sedimentary origin, with 
which are associated quartzites, slates, and some igneous rocks. In general the strike is 
N. 20" W., and the prevailing dip is westerly at angles ranging from 15° to 20°. A great 
thickness of coarse Tertiary conglomerate lies high up on the northeastern flanks of the 
range, but at the southeastern end of the crystalline area Paleozoic sediments abut against 
the older series and dip southeastward. 

An outlying mass of nearly horizontal coarse Tertiary conglomerate, composed chiefly of 
pebbles of limestone and quartzite, caps the spur of the mountains north of Salt Lake City 
and conceals the older sediments except along the western base of the spur, where the 
Wasatch limestone outcrops. A small isolated body of volcanic rock outcrops in the midst 
of the Tertiary area and is bisected by City Creek. The headwaters and upper course of 
City Creek lie in Paleozoic rocks, chiefly in the Weber quartzite and Wasatch limestone, 
which dip southeastward at angles varying from 30° to 65°. Across the divide a large area 
of fla,t-lying Tertiary rocks cap the disturbed Paleozoic series. 

aBoutwell, J. M. Progress reports Park City mining district: Bull. U. S. Geol. Survey No. 213, 1903, 
pp. 31-40; No. 225, 1904, pp. 141-150; No. 260, 1905, pp. 150-153. Economic geology Bingham mining 
district: Prof. Paper U, S. Geol. Survey No. 38, 1905 (with a section on areal geology by Arthur Keith 
and an introduction on general geology by S. F. Emmons). 



GEOLOGY. 9 

Between City and Big Cottonwood creeks the summit and western face of the mountains 
are occupied by an immense syncline striking nearly east and west. Its western end is 
terminated by the Wasatch fault, which cuts directly across the fold and exposes the struc- 
ture so that it can be plainly seen from Jordan Valley. The axis of the syncline coincides 
approximately with the course of Emigration Creek. In detail, however, the structure is 
complicated by a number of relativ(Jy minor disturbance s. 

East of Salt Lake City upper Carboniferous and Permian strata, consisting chiefly of lime- 
stone, outcrop between City and Red Butte creeks, and dip southward, forming t\w northern 
limb of the syncline. Red Butte Canyon lies in Permo-Carboniferous rocks, but near the 
mouth of the canyon "Red Beds" outcrop and continue along its southern divide. The 
"Red Beds" consist chiefly of red shales and sandstones, aggregating over 1,000 feet in 
thickness and are overlain by thin-bedded, argillaceous limestones and shales of Jurassic 
age. These rocks occupy the center of the syncline, and outcrop in the valley of Emigration 
Creek. 

South of Emigration Creek the summit and western face of the Wasatch Mountains are 
occupied by the southern limb of the syncline as far as Big Cottonwood Creek, and the 
succession of rocks mentioned above is repeated in reverse order. The dips generally are 
northward, but there are minor folds and faults. 

Parleys Creek rises in the Cretaceous sandstone and conglomerate that, east of the main 
Wasatch ridge, lie unconformably upon the older rocks. After traversing this area it crosses 
a narrow belt of Red Beds and, for 5 miles above the mouth of its canyon, flows over calcare- 
ous and argillaceous Permo-Carboniferous rocks. Carboniferous strata occupy the divide 
between Parleys and Mill creeks, the latter of which flows for the greater part of its length 
in the Weber quartzites. 

Between Mill and Big Cottonwood creeks the lower Paleozoic rocks outcrop. Big Cotton- 
wood Creek exposc^s for 6 miles above the mouth of its canyon a great thickness of Cambrian 
strata, consisting of siliceous slates and quartzites; in the upper part of its course this creek 
crosses the Weber quartzite and Wasatch limestone, and heads in the crystalline rocks of 
Clayton Peak. Little is known of the occurrence of Silurian and Devonian sediments in 
this area. Their presence was recorded by the early surveys, but the little detailed work 
that has been done shows that in a few localities at least these systems do not appear to be 
represented by sediments. 

Little Cottonwood Creek for about 8 miles from the mouth of its canyon flows through a 
crystalline area, and heads in Paleozoic strata and igneous rocks at the foot of Clayton 
Peak. The western base of the mountains extending north and south of Little Cottonwood 
Creek is occupied by a belt of schistose rocks about 10 miles long and averaging perhaps 1 
mile in width. These rocks are of pre-Cambrian age and are over a thousand feet thick. 
They consist largely of quartzite, but include also slates and mica-schists, having an appar- 
ent steep western dip. Up Little Cottonwood Creek, beyond the pre-Cambrian area, lies 
a large body of granitic rocks, which forms high peaks north and south of the creek, and 
through which the stream flows for the greater part of its course. The Paleozoic sediments 
arch around this granitic area, dipping away from it to the north, east, and south, forming 
a dome the western part of which has been cut ofl' by the Wasatch fault. 

The age of the "Little Cottonwood granite " has been the subject of some discussion. It 
clearly cuts the pre -Cambrian rocks at the mouth of the canyon, but its relation to the 
Cambrian was not definitely determined by the early surveys, though the granite was 
thought to be of pre-Cambrian age. Recently, however, it has been shown a that the 
"granite" is an intrusive mass that cuts the Cambrian quartzite, though the age of the 
intrusion is not yet known. 

Partial topographic connrction between the Wasatch and Oquirrh ranges is maintained 
by the Traverse Mountains near tlu' head of Jordan Valley, but this connection furnish(>s 
little information concerning the relations of the two main mountain masses, because the 



o Emmons, S. F., Am, Jour. Sci., 4th sor., vol. U\, August, 19(«, j). 139. 



10 UNDERGKOUND WATER IN VALLEYS OF UTAH. 

Traverse Mountains are largely composed of younger lavas, which conceal the rocks upon 
which they lie. 

In the '' narrows " where Jordan River flows through the Traverse Mountains, practically 
horizontal Pleistocene gravels, which form the great embankment at the point of the 
mountain, are unconformably underlain near the river level by fine-textured sediments 
that dip southeastward at an angle of 40°. The lower part of these sediments consists of 
light calcareous clay and the upper part of fine sand and gravel. No fossils were found, but 
the marked unconformity and the character of the material suggest that the age of the 
lower deposits is Tertiary. 

East of Utah Lake the great Wasatch fault is impressively shown by the remarkable 
alignment of the base of the mountains extending from Spanish Fork Canyon to the Trav- 
erse Mountains in an approximately straight line, and by the abrupt rise of the mountains 
above the broad valley. Second and third lines of faulting, lying parallel to the main fault 
and east of it, are suggested by the topography, which rises steplike, with two intervening 
treads between the ascents, to the top of the main ridge, and by the unusual thickness of 
limestone exposed, which apparently requires repetition by faulting for the explanation of 
its occurrence. 

In this part of the range a disturbed belt of rocks with prevailing steep westerly dips 
occurs along the western base of the mountains, beyond which the strata dip eastward at 
low angles and the summits of the main ridge are capped by limestone lying almost flat. 
The streams that cross the mountains, therefore, flow transversely to the strike of the rocks, 
in marked contrast to the creeks farther north, whose courses lie approximately parallel to 
the strike. 

Excellent sections can be measured along the canyons, but very little detailed work 
has yet been done. The rocks in general are quartzite and limestone of Carboniferous age, 
but locally Cambrian sediments also occur. In Rock Creek Canyon, east of Provo, in the 
lower end of the gorge, the rocks are much disturbed and are complexly folded. Here a 
considerable thickness of white quartzite outcrops, overlain by a great mass of limestone. 
In a thin bed near the base of the limestone G. H. Girty obtained a few Cambrian fossils, 
and about 600 feet above, in massive. gray limestone, the beds being apparently conformable, 
he found Lower Carboniferous fossils. 

South of Hobble Creek easterly dips prevail from the base of the mountains as far as 
Spanish Fork, beyond which the range has been very little studied. It trends southwest- 
ward and terminates at Mount Nebo, the main mass of which is composed of steeply west- 
dipping limestone and subordinate quartzite of upper Carboniferous age. The highland 
farther south consists of a series of plateaus, which are underlain by low-lying Mesozoic and 
Tertiary rocks. 

The highlands that border the valleys of Jordan River and Utah Lake on the west are for 
the most part composed of the same rocks that occur in the Wasatch Mountains, but the 
structural relations are completely hidden by the deep filling of the intervening valleys. 

The Oquirrh Range is composed mainly of Carboniferous limestones and quartzites, 
which, in the southern part of the mountains, are folded into two parallel anticlines with an 
intervening syncline. The axes of folding are obliquely transverse to the topography, the 
range extending in a north-south direction while the structural trend is northwestward. 
The structure of the northern part of the mountains is little known, but the range is proba- 
bly terminated by a fault. Rocks of Cambrian age are exposed locally by a fault in the 
vicinity of Mercur, and igneous rocks, both extrusive and intrusive, also occur. The 
intrusive rocks include both acidic and basic porphyries, which are conspicuous in the 
vicinity of the mining camps of Bingham and Mercur; the extrusive rocks, largely andes- 
itic, occur principally along the eastern base of the range and in the Traverse Mountains. 

The Lake Mountains, or Pelican Hills, west of Utah Lake, are composed of Carbonif- 
erous limestones and quartzites which constitute a low synclinal fold, and are separated 
from the Traverse Mountains by a narrow strip of Pleistocene deposits. A line of hills, 



GEOLOGY. 11 

composed chiefly of west-dipping limestone, separate the Lake Mountains from the East 
Tintic Range — the succeeding highland mass to the south. The northern end of these 
hills is capped by horizontal basalt with which light pumiceous tuff is associated. 

The East Tintic Range, a complex mass of sedimentary and igneous rocks, forms the 
southwestern border of Utah Lake basin. As in Rock Canyon, the sediments consist of 
Cambrian quartzite and Carboniferous limestone in juxtaposition, indicating the al)sence. 
of the Ordovician, Silurian, and Devonian. The main structure of the sedimentary rocks is 
synclinal, but these constitute a relatively small part of the outcrops, igneous rocks, rhyo- 
lite, andesite, monzonite, and basalt occupying most of the region. These are of both 
extrusive and intrusive origin, and are of Tertiary age. The low spur of the Tintic Moun- 
tains known as Long Ridge, which lies south of Goshen and connects with the Wasatch — save 
for a narrow Pleistocene strip south of Santaquin — consists of andesite in its southern part, 
while southeast-dipping Carboniferous limestones outcrop in the gorge of Currant Creek. 

T.ATE GEOLOGIC HISTORY. 

The above resume implies for this region a complex geologic history which need not here 
be discussed. A statement of late geologic events will, however, add to a clearer under- 
standing of the valley deposits in which the underground water is stored. 

TERTIARY HISTORY. 

After many thousands of feet of sediments had accumulated in Paleozoic and Mesozoic 
time, during which the general region was occupied by oceanic waters, profound continental 
uplift occured in early Tertiary time. Since then the ocean has not invaded the interior of 
the continent and during Tertrary time much of the Cordilleran region is believed to have 
been occupied by a number of lakes in which a considerable thickness of rocks accumulated. 
During the Eocene, according to the geologists of the Fortieth Parallel Survey, a great fresh- 
water lake occupied the Wasatch Mountain area, and toward the close of this epoch the 
mountains were finally uplifted and the relative depression of the Great Basin originated. 
The late Tertiary witnessed the formation of several lakes whose positions were determined 
by different crustal movements, and these lakes persisted with varying relations into the 
Pleistocene epoch. The end of Tertiary time was marked by further earth movements that 
divided the Great Basin area into two main depressions, following the bases of the recently 
uplifted Wasatch Mountains and the Sierra Nevada. In Quaternary time the bordering 
mountains were occupied by glaciers, and enormous lakes accumulated in the marginal 
depressions of the Great Basin. The two largest of these have been named after early 
explorers. Lake Lahontan covered an immense area in western Nevada and Lake Bonne- 
ville occupied a considerable part of western Utah and extended into adjacent parts of 
Nevada and Idaho. 

QUATERNARY HISTORY. 

The existence of Lake Bonneville is borne witness to by a number and variety of facts, 
chief of which are the remains of shore lines and shore deposits, and the great thickness of 
sediments that accumulated in the lake and that now constitute the valley floor. At its 
greatest extent the water of Lake Bonneville was approximately 1,000 feet above the 
present surface of Great Salt Lake. This large body of water abutted against the adjacent 
highlands and the outline of the lake was intricate. Deep bays and jutting promontories 
marked the shores, and lone mountains, partly submerged, stood out as islands. 

The area considered in this report formed part of one of these bays. This — 

was divided by a close stricture into an outer bay and an inner, the outer covering the valley of the 
Jordan River and the inner spreading over Cedar, Utah, and tJoshen valleys and a part of Juab Valley. 
In the inner bay the Goshen Hills made two islands, and the Pelican Hills constituted one large 
and several small islands. Small estuaries occupied Emigi-ation and Little Cottonwood canyons, 
connecting with the outer bay, and the inner bay sent an estuary into Provo Canyon.a 



a Gilbert, G. K., Lake Bonneville: Men. U. S. Geol. Survey, vol. 1, 1890, p. 103. 



12 UNDERGEOUND WATER IN VALLEYS OF UTAH. 

During the existence of Lake Bonneville sedimentation was practically continuous in its 
lowest depression, but toward the periphery oscillations of the water level alternately cov- 
ered the lake deposits and exposed them to subaerial influences. Evidence of the earliest 
Pleistocene history of the Bonneville region is furnished by alluvial cones that extend nearly 
to the bottom of the basin. These are composed of detritus derived from the adjacent 
highlands under subaerial conditions and could not have been accumulated when the level 
of the lake was high. It is therefore concluded that at this early period in the history of 
the lake comparatively arid conditions prevailed, for the stage of a lake in a closed basin is 
determined by the relation of evaporation to water supply. It has also been determined 
that at this period of the history of the lake it had no outlet and that the time of duration 
of low water was relatively long. 

Next succeeded a period of high water, when yellow clay, locally streaked with sand, 
was deposited in a large part of the lake. The base of the yellow clay has not been observed 
and good sections are rare, though an exposure 150 feet thick has been measured. The 
deposit locally extends to within 120 feet of the highest level attained by Lake Bonneville, 
but a study of the shore line shows that during the deposition of the yellow clay the water 
did not rise to the rim of the basin. In the lower part of the basin the yellow clay is 
unconformably overlain by a deposit of white marl, local streaks of alluvium occurring 
at the contact. The white marl is composed of a fine calcareous clay consisting of calcium 
and magnesium carbonates, microscopic siliceous organic remains, and fine clastic debris. 

These facts imply (1) that after the deposition of the yellow clay the lake water sub- 
sided, (2) that the clay was eroded, and (3) that a second period of high water subsequently 
ensued when the white marl was deposited. The extent to which the waters subsided is 
undetermined, but the possibility of complete desiccation is suggested by the difference 
in character between the yellow clay and white marl. The extent of the second period of 
high water is determined by the highest shore line traceable along the adjacent mountain 
flanks. This level is approximately 1,000 feet above Great Salt Lake and is known as the 
Bonneville shore line. The lake then outflowed through Cache Valley into the Snake 
River basin. 

The Bonneville shore line marks the highest stage of Lake Bonneville and the level of 
its initial outflow. Beneath this level the drainage channel was cut down by the outflow 
of the lake to a depth of approximately 375 feet. That the lake maintained its level at the 
stage of lowest outflow for a relatively long time is attested by the well-developed shore 
phenomena at the corresponding elevation. This stage determined the Provo shore line, 
so named from its great development near that town. 

The present conditions have been brought about by the recession of the lake's surface, 
due to the excess of evaporation over inflow, so that now Great Salt, Utah, and Sevier lakes 
are the sole remnants of the former great body of water. The recession has uncovered the 
great expanse of lake beds that underlie the intermontane plains and constitute the fertile 
lands at the base of the Wasatch Mountains, and has also exposed the remarkable shore 
phenomena that testify to the history of Lake Bonneville, so completely worked out by 
Gflbert. 

The Bonneville basin is preeminently characterized by its many shore lines (PI. Ill, B), 
the highest of which impinges against the mountains and the lowest of which that can be 
recognized incloses the area covered by the lake sediments. Through a vertical interval 
of 1,000 feet the story of the rise and fall of this body of water is recorded by the super- 
position of shore line upon lake sediment and of lake sediment upon shore line. The record 
is not in all cases perfectly legible, but the main features are unmistakable. 

The work of waves is recorded by cliffs and wave-cut terraces, from which the debris 
was carried along the shore to make benches, bars, spits, and terraces. The streams loaded 
with the waste of the land areas deposited their burdens in the lake, the coarser detritus 
being laid down near shore while the finer sand and clay were carried far out before sedi- 
mentation occurred. Deltas were formed at,the mouths of the larger creeks where so much 
debris was carried that the shore currents could not distribute it. Since the recession of 




A. NORTHERN END OF UTAH LAKE. 
Oquirrh Mountains in background. 




7;. HEAD-GATE OF JORDAN AND SALT LAKE CITY CANAL, LOOKING SOUTH. 
Embankment at point of the mountain in background. 



GEOLOGY. 13 

the lake from its old shores the streams which formed the deltas have begun their destruc- 
tion by cutting them in two in their progress toward the shrunken body of water. 

The Bonneville is the most conspicuous of all the shore lines, not because of the relative 
duration of time during which it was formed but because being the topmost of the series, 
it emphasizes the contrast between the sharply carved subaerial erosion features of the main 
land and the broad horizontal lines due to the influence of the lake. Study of the levels 
of bars at this stage shows that the record is complex and that the water surface alter- 
nately rose and fell a few feet during the formation of the shore phenomena that mark the 
general Bonneville level. 

Below the Bonneville there are a number of plainly marked shore lines which represent 
stages in the level of the lake when it was practically constant for relatively long periods. 
Of these shore lines the Provo is the most remarkable, for it records the longest occupancy 
of one approximate horizon of any of the stages of the lake. Its embankments are the 
most massive and its wave-cut terraces are the broadest, notwithstanding the fact that the 
lake at the Provo stage was considerably smaller than when the surface of the water was 
375 feet higher, its area having shrunk from 19,500 to approximately 13,000 square miles. 
The Provo shore line is characterized particularly b}^ its deltas, which were formed at the 
mouths of all the larger streams that entered the lake. 

The fall from the Bonneville to the Provo level was apparently without interruption and 
comparatively rapid. But below the Provo stage there are remnants of shore lines and 
terraces at a number of horizons that record temporary halts of greater or less extent in the 
gradual shrinkage of the lake. The most conspicuous of these lower shore lines, at an 
elevation of approximately 750 feet below the Bonneville level, has been named the Stans- 
bury shore line, from its prominent development on Stansbury Island, but the others have 
not been correlated. As many as ten distinct shore lines can be traced on the west side 
of Jordan Narrows. 

In connection with the different shore lines it is of interest to note that Gilbert has found 
evidences at a few localities of oscillations of the lake level between the Provo and Bonne- 
ville horizons, which appear to record halts in the rise of the lake as it approached its 
maximum. This is unusual, for most of the observed shore phenomena were formed during 
the retreat of the lake. 

Local deposits of calcareous tufa occur associated with the various shore lines, but are 
most abundant at the Provo horizon. The tufa appears to have been deposited by precipita- 
tion from the lake waters due to aeration of the waves, especially during storms, and con- 
sequent loss of carbon dioxide by which the carbonate of lime was held in solution. The 
tufa occurs as a cement to gravel and as a more concentrated deposit, from a few inches to 
a few feet in thickness, coating exposed surfaces. 

Below the Provo horizon, lake beds consisting of subhorizontal or gently lake ward-sloping 
sediments are associated with shore deposits until, as the valley bottom is approached, 
shore markings become indistinct and the lake beds prevail. The deposits of yellow clay 
and white marl previously mentioned as being widely distributed in the Bonneville basin 
apparently are not typically developed in the bay of the old lake, which occupied the area 
under consideration. A number of deep wells have been sunk into the valley deposits and 
their records indicate the general composition of the sediments (PI. V). The beds are at 
least 2,000 feet thick, and consist of gravel, sand, and clay, which constitute the reservoirs 
in which ground water is stored. 

CLIMATE. 

Weather observations have been systematically recorded at Salt Lake City for thirty- 
one years, and at near-by stations, including Provo, Thistle, Heber, and Park City, for 
eight to fourteen years. The most important meteorologic data, compiled from reports of 
the United States Weather Bureau, are summarized in the following tables, which give 
details of precipitation, temperature, wind velocity, humidity, and evaporation, on which 
the supply of underground water directly depends. 



14 



UNKEBGROUND WATER IN VALLEYS OF UTAH. 



PRECIPITATION^. 

Monthly and annual precipitation at Salt Lalce City, 1875 to 1904.. 
[Inches.] 



Year. 



Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Dec. Annual 



1875. 
1876. 
1877. 
1878. 
1879. 
1880. 
1881. 
1882. 
1883. 
1884. 
1885. 
1886. 
1887. 
1888. 
1889. 
1890. 
1891. 
1892. 
1893. 
1894. 
1895. 
1896. 
1897. 
1898. 
1899. 
1900. 
1901. 
1902. 
1903. 
1904. 



3.05 
1.23 

.87 
1.07 
1.87 

.29 
1.24 
1.50 
1.47 

.71 
1.48 
1.91 
2.36 
1.52 

.73 
3.67 

.74 
1.61 

.82 
1.31 
1.32 
1.26 
1.16 

.58 

.84 

.44 

.95 



2.11 
1.45 



0.79 

1.52 

.38 

3.49 

.71 

1.02 

2.44 

.42 

.72 

2.23 

1.56 

1.36 

1.41 

1.22 

.81 

2.05 

.76 

.68 

1.64 

.83 

.85 

.69 

3.81 

.38 

2.98 

1.30 

1.77 

1.17 

.82 

2.25 



Mean. 



1.44 



1.33 



2.81 
4.00 
2.93 
2.54 
.67 
.43 
.88 
1.12 
1.75 
3.69 
2.64 
2.60 
-.35 
2.18 
1.64 
1.12 
4.66 
2.21 
2.68 
1.73 
.81 
1.99 
2.20 
1.71 
2.93 
.33 
2.48 
1.22 
1.35 



1.50 
2.09 
2.14 
2.63 
3.26 
2.37 
2.37 
3.81 
2.92 
2.89 
3.47 
4.43 
1.87 

.99 
1.52 

.94 
1.49 
1.90 
2.72 
1.67 

.73 
2.53 
2.00 
1.30 

.81 
2.91 

.87 
3.69 
1.11 
2.20 



2.91 

4.30 

3.49 

2.50 

.10 

1.85 

2.55 

.26 

.98 

1.78 

2.49 

.06 

.73 

.34 

2.97 

.16 

.72 

1.65 

1.68 

1.22 

2.29 

3.67 

.98 

4.19 

2.50 

.44 

4.27 

.33 

3.55 

3.08 



0.90 
.09 
.80 
.35 

1.34 
.01 
.28 

2.24 
.33 
.33 

2.67 

1.02 
.37 
.98 
.01 
.32 

1.08 

1.21 
.04 

1.38 
.99 
.25 
.52 

1.45 
.96 
.08 
.49 
.37 
.74 
.27 



1.01 
.83 
.02 

1.08 
.07 
.20 
.21 
.30 
.10 
.27 
.58 

T. 

1.23 
.24 
.08 
.02 
.47 
T. 

1.19 
.82 
.42 

1.35 
.69 
.18 
.42 
.32 
.31 
.56 
.14 
.59 



0.25 
.92 
.28 
.81 
.06 
.74 

1.61 

1.61 
.62 
.73 
.90 
.59 
.69 
.63 
.92 
.79 
.46 
.05 
.71 
.87 
.02 

1.47 
.33 

1.35 

1.06 
.72 

1.22 
.15 
.43 



1.22 

.42 

.90 

3.15 

.01 

.56 

.43 

.37 

.13 

1.91 

1.29 

1.88 

.55 

.51 

.52 

T. 

1.19 

.12 

1.30 

2.87 

.95 

.52 

.48 

.15 

T. 

1.44 

.66 

.05 

.84 

.12 



1.36 
3.27 
2.41 
1.39 
1.62 
.40 
2.19 
2.89 
2.24 



.30 

.80 

3.85 

1.44 

1.26 

1.58 

1.02 

1.01 

.24 

.70 

1.91 

1.57 

2.85 

1.99 

.98 

.52 

.81 

1.18 



5.81 

.81 
1.02 

.63 

.32 
1.17 
1.44 

.54 
1.78 

.50 
3.10 
1.79 

.25 
2.00 
1.04 

T. 

.90 

.72 
1.18 

.28 
2.44 
3.15 
1.19 
1.95 
1.52 
1.40 

.92 
1.24 
2.21 

.00 



2.03 
1.80 
1.11 

.11 
3.08 
1.90 
1.24 

.92 
1.20 
2.12 

.92 
1.27 
1.55 
2.21- 
4.37 

.42 
2.19 
2.35 
2.37 
1.28 

.89 

.84 
1.47 
1.28 

.61 

.16 
1.16 
1.31 

.51 

.90 



2.03 



2.21 



1.62 



,79 



53 



1.54 



1.36 



Monthly and annual precipitation at Parle City, 1899 to 1904- 
[Inches.] 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 


Deo. 


Annual. 


1899 






















0.90 
3.50 
1.40 


1.80 
1.30 
2.20 




1900 


0.93 
2.24 
1.90 
3.88 
2.15 


1.87 
2.35 
1.18 
1.34 
5.00 


0.38 
3.15 
4.04 
2.60 

7.85 


3.56 
1.92 
1.96 
.95 
1.69 


0.30 
1.50 

.67 
2.89 
2.44 


T. 
0.20 


0.10 
.90 


0.32 
1.40 


2.23 
.45 


0.90 

.18 


15.39 


1901 


17.89 


1902 




1903 


T. 






.92 


.30 


.55 
.00 


.95 




1904 




1.99 



















CLIMATE. 



15 



Monthly and annual precipitation at Provo, 1899 to 1904^. 
[Inches.] 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. Aug. I Sept. 


Oct. Nov. 


Dec. 


Annual. 


loqq 


1.54 
.45 
.22 
.35 
2.65 
1.72 


2.89 
.35 

2.06 

1.12 
.65 

2.27 


2.45 
.05 
1.09 
1.30 
1.80 
3.75 


0.39 
1.65 

.29 
2.14 

.51 
1.56 


1.37 

.32 

.39 

.36 

2.69 

2.11 








0.00 
1.13 


2.79 
.66 
T. 
.68 
.55 


0.94 
3.50 

.85 
1.55 
1.14 

.00 


1.05 
.12 
.98 

1.28 
.49 

1.05 














loni 


0.18 
.10 
.30 

.42 


T. 

0.11 

.39 

.39 







1902 


0.20 
.42 
.45 


.72 




1903 


12.31 


1904 


.04 1.56 


15.32 











Monthly and annual precipitation at Heher, 1899 to 190Ji.. 
[Inches.] 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. Oct. 


Nov. 


Dec. 


Annual. 


1899 


2.95 


5.85 


3.00 


0.89 


1.14 


0.97 


1.61 


2.10 


1 
0. 15 3. 20 0. 85 


1.55 


14.26 


1900 


1.06 


1.50 


.34 


2.53 


.16 


.20 


.25 


.31 


1.20 1.47 


4.42 


.22 


13.66 


1901 


2.20 


2.20 


1.56 


.31 


1.72 


.08 


. 40 2. 06 


. 16 1. 70 


1.40 


1.50 


15.29 


1902 


.50 
2.17 
2.10 


1.03 

.07 

3.00 


1.46 
1.95 
3.48 


1.88 

.78 


.49 
1.42 


.37 
.25 
.73 


. 15 . 50 
.69 .02 

.29 1 .88 


. 45 . 45 

1.17 .76 

. 16 ! 1. 22 


1.77 

1.90 

.00 


1.04 
1.33 
1.91 


10.09 


1903 


13.32 


1904 


.96 2.01 


16.74 



























Monthly and annual precipitation at Thistle, 1899 to 190^. 
[Inches.] 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 


Dec. 


Annual. 


1899 


1.60 
.30 


2.40 

.47 

2.35 

2.05 


1.30 

.00 

2.40 

2.00 


0.05 
1.77 
1.15 
2.23 
1.75 
.90 


0.88 
.05 
.85 
.35 
1.60 
2.65 


T. 
0.10 
.05 
.00 
.35 








0.40 
.75 

1.15 
.41 

1.43 
.27 


2.08 

1.80 

.93 

2.10 

.80 

.00 






1900 


0.10 
.11 
.35 
.53 
.32 


0.46 

3.05 

.20 

.10 

.46 


1.00 
.25 
.85 
.66 

1.90 


0.30 
2.00 
1.45 
1.40 
1.50 


7.10 


1901 




1902 


i.« 


13.89 


1903 




1904 


1.90 


1.55 







TEMPERATURE. 

Mean monthly and annual temperature at Salt Lake City, 1873 to 1904. 



January 27. 9 

February 33. 

March 41.6 

49.5 



April. 
May. 
June. 
July. 



57.8 
67.0 

75.5 



August 74. 8 

September 64. 3 

October 52. 3 

November 39.8 

December 32. 7 

Annual 51. 4 



Mean monthly and annual temperature at Provo, 1890 to 1904- 



January 26. 6 

February 29. 3 

March 39 . 3 

April 49. 1 

May 58. 

June 64. 7 

July 73.2 



August 70. 7 

Soptomhor 59.8 

October 48. 7 

November 38. 4 

Doceml)er 29.2 

Annual 49. 2 



16 UNDERGROUND WATER IN VALLEYS OF UTAH. 

Monthly maximum temperature at Salt Lake City, 1899 to 1904. 











[°r.] 
















Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 


Dec. 


1899 


54 
57 
51 
43 
53 
48 


51 
55 
55 
62 
42 
66 


67 
72 
65 
58 
65 
63 


80 

78 
79 
78 
80 
78 


83 
89 
88 
88 
86 
83 


96 
101 
90 
98 
91 
92 


97 
99 
101 
96 
96 
97 


91 
94 
95 
98 
98 
94 


91 
88 
86 
92 
92 
92 


73 
76 
85 
81 

77 
83 


63 
68 
67 
70 
70 
66 


59 
56 
59 


1900 


1901 


1902 


58 
45 
55 


1903 


1904 .... 






Mean 


51 


55 


65 


79 


86 


95 


98 


95 


90 


79 


67 


55 





Monthly minimum temperature at Salt Lake City, 1899 to 1904. 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 


Dec. 


1899 


16 

20 

4 

- 4 

15 

7 


-10 
10 
15 
12 

- 4 
6 


20 
26 
25 
21 
14 
19 


30 
30 
15 
32 
25 
30 


25 
40 
43 
35 
33 
36 


34 
47 
40 
42 
54 
44 


51 
53 
49 
43 
46 
51 


46 
52 
56 
52 
48 
46 


46 
32 
39 
35 
37 
38 


30 
27 
36 
36 
32 
28 


28 
28 
29 
21 

I 


9 
2 


1900 


1901 


11 


1902 


15 


1903 


14 


1904 


7 






Mean 


11 


10 


21 


■ 27 


35 


44 


49 


50 


38 32 


25 


10 











TVIND VELOCITY. 

Average wind velocity at Salt Lake City, 1900 to 1904- 
[Miles per hour.] 



Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. Nov. 


Dec. 


Annual. 


1900 


3.4 
5.0 
3.8 
4.8 
4.1 


5.2 
4.0 
5.5 
4.5 
6.3 


6.3 
6.2 
6.9 
6.8 
7.3 


7.3 

7.8 
6.7 
7.3 
7.2 


6.8 
7.3 
7.1 
6.1 

6.8 


6.5 
6.6 
6.7 
6.6 
6.5 


6.0 
6.3 
6.7 
7.2 
6.5 


6.4 
5.8 
6.5 
6.2 
5.7 


6.5 
7.0 
6.7 
6.3 
6.0 


6. 5 5. 
5. 4. 9 

5. 7 1 6.0 


4.5 
4.8 
4.7 
3.7 
4.9 


5.9 


1901 


5.9 


1902 


6.1 


1903 


5.3 
5.4 


5.4 

4.7 


5.8 


1904 


6.0 






Mean 


4.2 


5.1 


6.7 


7.2 


6.8 


7.0 


6.5 


6.1 


6.5 


5.6 


5.2 


4.5 


5.9 



HUMIDITY. 

Mean relative humidity at Salt Lake City, 1900 t@ 1904- 
[Per cent.] 



c 




























Year. 


Jan. 


Feb. 


Mar. 


Apr. 


May. 


June. 


July. 


Aug. 


Sept. 


Oct. 


Nov. 

62 
57 
56 
64 
45 


Dec. 


Annual. 


1900 


78 
69 
83 
73 

75 


65 
73 

62 

74 
62 


40 
55 
58 
52 
64 


59 
42 
48 
44 
46 


41 
44 
43 

48 
49 


25 
36 
31 
38 
38 


24 

26 
27 
30 
33 


24 
39 

27 
28 
38 


36 
30 
32 
38 
34 


48 
50 
40 
45 
53 


63 
71 
65 
75 
60 


47 


1901 


49 


1902 . .. 


48 


1903 


51 


1904 


5® 






Mean 


76 


67 


54 


18 


45 


34 


28 


31 


34 


47 


57 


67 


49 



CLIMATE. 
K^' APOll^VTlON . 

Depth of evaporation at Utah Lake a from August, lOOS, to August, 190 Jf. 



17 



[Inches.] 



1903. 



August 8. 40 

September (J. 78 

October 3. 86 

November 2. 50 

December 1-50 

1904. 

January 1.50 



1<K)4— Continued. 

February 2. 00 

March 3. 50 

April 4. 63 

May 7. 72 

June 8. 80 

July 9.41 



Total. 



SUMMARY. 



The climate of the valleys of Utah Lake and Jordan River is controlled by their location 
in the central eastern part of the Great Basin, but is modified somewhat by the proximity 



^5 
20 




' 


1 










1 


1 








1 






1 




15 










1 




1 










1 












1 


























1 












1 










1 






10 


- 


- 


- 


- 






- 


- 


- 


- 


- 






- 










- 


- 






- 


- 






- 






- 


- 


5 

o 


~ 


- 


~ 


- 






- 


- 


- 


- 


- 






- 










- 


- 






- 


- 






- 


- 




- 


- 






5S !i; S S> o 






Fig. 1.— Diagram showing variation of annual precipitation at Salt Lake City. 



of Utah and Great Salt Lakes and the Wasatch Mountains. The tables show that the 
climate is characterized by low annual precipitation, moderate temperature, moderate 
wind velocity, low relative humidity, and considerable evaporation. 

The mean annual precipitation at Salt Lake City is 10.19 inches, ranging between a maxi- 
mum of 23.64 inches in 1875 and a minimum of 10.33 inches in 1890. Since 1900 it has 
averaged 2.2 inches below normal (fig. 1). Only about 18 per cent of the annual total 



o Computed from daily mciisurements of a tank 3 feet in diameter. Tests were made by the engi- 
neer of Salt Lake City from 1901 to 1903. and since then they have been kept up by the Reclamation 
Service under G. L. Swendsen. See also Newell, F. II., Fourteenth Ann, Rept. U. S. Ceol. Survey, 
pt. 2, 1894. p. 154. 

IRK 157—06 2 



18 



UT^DERGKOUND WATER IN VALLEYS OF UTAH. 



occurs from June to September, and for these four months amounts to less than 3 inches. 
Between October and May the variation is not marked, but the greatest precipitation 
occurs in March and April (fig. 2). This precipitation is unusually high for the Great 
Basin. The Wasatch Mountains serve to condense the moisture, originally derived in large 
part from the westerly winds from the Pacific Ocean, that remains in the air after crossing 
the Sierra Nevada. 

Probably the precipitation is greater on the summits than at the stations where records 
have been kept, but data are not available. The melting snow of the winter's accumulation 
is ihe chief supply of the streams of the area under consideration. 

The mean annual temperature of -Salt Lake City is 51.4°. The mean monthly maximum 
ranges from 98° in July to 51° in January, while the mean monthly minimum varies between 
10° in December and February and 50° in August. 

The dryness of the atmosphere is indicated by the mean relative humidity of 49 per cent, 
varying from 28 per cent in July to 76 per cent in January, and by the amount of evapora- 
tion from a free water surface, which, according to the latest measurements, is about 60 



Per 

cent 

14- 


Jan. 


Feb. 


Mar 


Apr 


May 


June 


July 


Aug. 


Sept. 


Oct. 


Nov. 


Dec. 




























/2 


























































10 






















, 








- 






































e 






















■ 


























































6 




















































































4- 






























































































B 


























1 














































1 






















n 


























1 























Jnches 1.44 1.33 2.03 2.21 1.62 .79 .53 .72 .93 L54 1.36 /.64 
Fig. 2.— Diagram showing mean monthly precipitation at Salt Lake City. 



Mean 

annua/ 

I6./9 



inches a year. Yet the chmate is not nearly as dry as in other parts of the Great Basin. 
The dryness lessens the effect of the summer's heat, so that the "sensible temperature" is 
not so great as would be suggested by the thermometer, being modified by the cooling 
effects of evaporation. 

HYDROGRAPHY. 
STREAMS TRIBUTARY TO UTAH LAKE AND JORDAN RIVER. 

Seepage from surface streams, as shown hereafter, is the most important source of supply 
of underground water in the valleys of Utah Lake and Jordan River. A summary of 
discharge measurements therefore throws important light on the subject and, with other 
data, furnishes facts for roughly estimating the amount of water available for the annual 
replenishment of the underground reservoirs. The figures here given have been compiled 
from records of the United States Geological Survey and from data obtained through the 
courtesy of the city engineer of Salt Lake City, and are now published for the first time. 

Satisfactory measurements of the flow of all the streams in the two valleys have not been 
made. However, records have been kept for a number of years of the discharge of several 
of the more important, and the combined data, with due consideration for varying con- 
ditions, may be taken as typical of the drainage of the entire watershed. The measure- 



HYDROGRAPHY. 



19 



merits wore made at the mouths of the canyons. Below tliese points, (hiring the irrigation 
season, the water is diverted and conducted over the valley in an intricate .system of 
ditches, so that the stream beds in their lower stretches are then often dry. During the 
flood season the streams discharge directly into either Utah Lake or Jordan River. Fol- 
lowing are tables of monthly measurements for 1904, to which annual summaries for several 
years are added where figures are available: 

Estimated discharge {at mouths of canyons) of streams tributary to Jordan River and Utah 

Lake. 

CITY CREEK. 
[Drainage area, 19 square miles.] 



Date. 



1904. 

January 

February 

March 

April 

May 

June 

July 

August 

September. . . 

October 

November... 
December 



Year. 



1903. 
1902. 
1901. 
1900. 



Discharge. 



Maxi- 
mum. 



Sec. 



-feet. 

6.7 

7.9 

11.0 

28.8 

70.1 

57.0 

26.5 

15.3 

11.4 

9.3 

8.7 

9.2 



70.1 
63.1 
58.2 
72.0 
31.3 
121.9 



Mini- 


mum. 


Sec-feet. 


6.0 


6.0 


7.3 


11.0 


28.8 


26.6 


16.2 


11.5 


9.4 


8.7 


8.2 


7.7 


6.0 


4.3 


3.6 


5.0 


5.4 


3.2 



Mean. 



Sec. 



-feet. 
6.2 
6.6 
8.1 
22.1 
55.6 
39.2 
19.7 
13.4 
10.4 
9.1 
8.5 
8.0 



17.2 
13.0 
12.3 
12.7 
9.8 
20.0 



Total. 



A cre-feet. 

381 

380 

516 

1,315 

3,419 

2,332 

1,211 

824 

619 

609 

506 



12,604 
9,440 
8,910 
9,251 
7,054 

14,491 



Run-off. 



Per 
square 
mile. 



Sec-feet. 

0.326 

.347 

.442 

1.160 

2.926 

2.063 

1.037 

.705 

.547 

.479 

.447 

.421 



Depth. 

Inches. 

0.376 

.374 

.510 

1.294 

3.373 

2.301 

1.195 

.813 

.610 

.551 

.499 

.485 



Relation 
to rain- 
fall. 



Per cent. 

20.9 

10.3 
8.6 

66.7 
122.2 
852.2 
202.5 

71.9 
508.3 

46.7 



.908 


12.381 


.685 


9.323 


.647 


8.811 


.668 


9.126 


.517 


7.040 


1.053 


14.306 



53.9 



Rainfall.a 



Inches. 

1.80 

3.62 

5.92 

1.94 

2.76 

.27 

.59 

1.13 

.12 

1.18 

.00 

.90 



61.2 
63.1 
69.5 
53.9 
52.5 
80.1 



20.23 
14.77 
12.67 
16.94 
13.41 
17.85 



EMIGRATION CREEK. 

[Drainage area, 19 square miles.] 



1903. 

January 

February. . . 

March 

April 

May 

June 

July 

August 

September. . 

October 

Noveml)cr. . 
December. .. 

Year. . 



6.3 


0.7 


1.1 


()8 


0.058 


0.069 


2.3 


.8 


.5 


.6 


33 


.032 


.033 


3.1 


11.7 


.4 


. 3.0 


184 


.158 


.182 


9.2 , 


12.8 


3.7 


8.0 


476 


.421 


.470 


4.5.6 


19.3 


5.5 


9.5 


584 


.500 


.576 


17.9 


18.1 


4.0 


8.6 


512 


.453 


.505 


136.5 


4.0 


1.6 


2.8 


172 


.147 


.169 


120.7 


1.7 


.6 


1.0 


61 


.053 


.061 


14.2' 


1.1 


.6 


.8 


48 


.042 


.047 


5.3 


2.0 


1.1 


1.2 


74 


.063 


.073 


13.3 


3.2 


1.0 


1.3 


77 


.068 


.076 


5. 5 


.8 


.6 


. 7 


43 


.037 


.043 


5.9 


19.3 


.4 


3.2 


2,332 


.169 


2.304 


15. 6 



2.99 
1.08 
1.97 
1.03 
3.22 
.37 
.14 
.43 



1.38 
.73 



14.77 



1 The record of rainfall given under City, Emigration, Parleys, and Mill creeks is the mean precipita- 
tion for Salt Lake City and Park City; that under .Vmerican Fork and i'rovo River is for Provo and 
lleber; that under Spanish Fork is for Provo, Thistle, and Soldiers Summit. 



20 



UNDERGROUND WATER IN VALLEYS OE UTAH. 



Estimated discharge (at mouths of canyons) of streams tributary to Jordan River and Utah 

Lake — Continued. 

PARLEYS CREEK. 

[Drainage area, 50 square miles.] 



Date. 



1904. 

January 

February . . . 

March 

April 

May 

June 

July 

August 

September . . 

October 

November . . 
December . . . 

Year . . 

1903 

1902 

1901 

1900 

1899 



Discharge. 



Maxi- 
mum. 



Sec-feet. 

9.2 

18.1 

39.3 

207.3 

208.5 

137. 5 

41. 1 

20.2 

13.0 

13.7 

11.8 

10.8 



208.5 
133.7 

95.3 
109.5 

39.0 
227.5 



Mini- 
mum. 



Mean. 



Sec-feet. 

4.8 

4.2 

9.4 

69.8 

88.1 

28.5 

19.5 

11.8 

9.4 

11.8 



2.5 
2.1 
2.2 
3.0 
2.9 
4.0 



Sec-feet. 

7.1 

10.3 

19.6 

123.2 

168.5 

52.6 

26.1 

16.0 

11.4 

12.9 

10.3 

8.3 



38.9 
20.5 
16.7 
19. y 
12.6 
59.8 



Total. 



Acre-feet. 

437 

592 

1,205 

7,331 

10,361 

3,130 

1,605 

984 

679 

793 

613 

510 



Run-off. 



Per 
square 
mile. 



Sec-feet. 

0.142 

.206 

.392 

2.464 

3.370 

1.052 

.522 

.320 

.228 

.258 

.206 

.166 



28,240 
14,879 
12,116 
14,490 
9,0^8 
39,722 



.777 
.410 
.334 
.398 
.251 
1.196 



Depth. 



Inches. 

0.164 

.222 

.452 

2.749 

3.886 

1.174 

.602 

.369 

.254 

.297 

.230 

.191 



10. 590 
5.581 
4.544 
5.429 
3.431 

14. 884 



Relation 
to rain- 
fall. 



Per cent. 

9.0 

6.1 

7.6 

141.8 

140.8 

434.8 

102.0 

32.7 

211.7 

25.2 



21.2 



52.3 
37.8 
35.9 
32.0 
25.6 
83.4 



Rainfall. 



Inch 



es. 

1.80 

3.62 

5.92 

1.94 

2.76 

.27 

.59 

1.13 

.12 

1.18 

.00 

.90 



20.23 
14.77 
12.67 
16.94 
13.41 
17.85 



MILL CREEK. 
[Drainage area, 21 square miles. 



1904. 

January 

February... 

March 

April 

May 

June 

July 

August 

September . . 

October 

November. . 
December . . . 

Year . . 

1903 

1902 

1901 

1900 



13.0 
13.0 
13.0 
25.1 
58.2 
55.9 
29.7 
16.8 
15.9 
14.0 
13.0 

n.3 



58.2 
34.4 
39.5 
47.4 
30.8 
66.0 



6.6 

3.7 

9.3 

11.3 

25.1 

29.7 

20.8 

13.0 

13.0 

13.0 

11.3 

1.0 



LO 
2.9 
1.9 
L4 
L4 
2.4 



9.9 


609 


0.471 


9.9 


569 


.471 


11.2 


G89 


.486 


18.8 


1,120 


.895 


41.4 


2,545 


1.971 


40.9 


2,434 


1,948 


25.7 


1,580 


L224 


14.9 


916 


.710 


15.0 


893 


.714 


13.7 


842 


.652 


12.4 


738 


.590 


8.6 


529 


.410 



18.5 
12.3 
12.1 
12.9 
11.5 
19.6 



13, 464 
8,916 
8,753 
9,391 
8,296 

14, 193 



.878 
.586 
.575 
.615 
.549 
.932 



0.543 


30.2 


.508 


14.0 


.560 


9.4 


.999 


51.5 


2.272 


82.3 


2.173 


804.8 


1.411 


239.2 


.819 


72.5 


.797 


664. 2 


.752 


63.7 


.658 




.473 


52.5 


11. 965 


59.1 


7.964 


5.3.9 


7.814 


61.7 


8.383 


49.5 


7.466 


55.7 


12. 669 


77.1 



L80 

3.62 

5.92 

1.94 

2.76 

.27 

.59 

L13 

.12 

L18 

.00 

.90 



20.23 
14.77 
12.67 
16.94 
13.41 
17.85 



HYDROGRAPHY. 



21 



Estimated discharge (at mouths of canyons) of streams Uihutary to Jordan River ami Utah 

Lake — Continued. 



BIG COTTONWOOD CREP^K. 
[Drainage area, 48 square miles.] 



Dato. 



1902. 

January 

FeV)ruary . . . 

March 

April 

May 

June 

July 

August. 

September.. 

October 

November. . 
December . . . 



Year. 



1901. 



Discharge. 



Maxi- 
nuun. 



Sec-feet. 
27.6 
2S. 4 
27.7 
142.9 
369. 7 
309.5 
92.3 
38.9 
31.6 
29.0 
28.8 
29.3 



369.7 
407.3 



Mini- 
mum. 



Sec-feet. 
13.6 
17.2 
20.4 
27.0 
108.9 
91.7 
40.9 
28.4 
25.2 
21.4 
21.8 
10.1 



Mean. 



Sec-feet. 
23.1 
24.2 
24.6 
70.4 
210.2 
194.5 
62.2 
33.0 
27.9 
26.3 
24.8 
22.8 



Total. 



13.6 
11.3 



62.0 
68.3 



L cre-feet. 
1,421 
1,344 
1,513 
4,189 
12,925 
11,574 
3,825 
2,029 
1,661 
1,617 
1,476 
1,402 



44,976 
49,639 



Per 
square 
mile. 



Sec-feet. 

0.481 

.504 

.512 

1.470 

4.380 

4.050 

1.300 

.688 

.581 

.548 

.517 

.475 



Run-off. 



1.292 
1.422 



Depth. 

Inches. 

0. 555 

..525 

.590 

1.640 

5. 050 

4. 519 

1.499 

.793 

.648 

.632 

.577 

.548 



17. 576 
19. 381 



Relation I Rainfall, 
to rain- 
fall. , 



Per cent. \ Inches. 



AMERICAN FORK. 
[Drainage area, 66 square miles.] 



1904 

January 

February. . 

March 

April 

May 

June 

July 

August 

September. 

October 

November.. 
December. . 

Year. 



17 


15 


16.1 


990 


0.244 


0.281 


14.7 


L91 


16 


15 


15.4 


886 


.233 


.251 


9.5 


2.64 


24 


15 


19.1 


1,174 


.289 


.333 


9.2 


3.62 


109 


23 


46.9 


2,791 


.711 


.793 


63.0 


1.26 


379 


95 


216.0 


13,280 


3.27 


3.77 


183.0 


2.06 


310 


131 


201.0 


11,960 


3.05 


3.40 


596. 


.57 


147 


()() 


95.3 


5,860 


1.44 


1.66 


488.0 


.34 


- 64 


44 


52.8 


3,247 


.800 


.922 


140.0 


.66 


43 


35 


38.1 


2,267 


.577 


.644 


644.0 


.10 


41 


34 


35. 9 


2,207 


.544 


.627 


45.1 


1.39 


34 

28 


28 
18 


30.0 
25.3 


1,785 
1,556 


.454 
.383 


.507 
.442 




.00 


29.8 


1.48 


379 


15 


06.0 


48,000 


1.00 


13. 62 


85.0 


16.03 



.22 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



Estimated 



{at mouths of canyons) of streams tributary to Jordan River and Utah 
Lalce — Continued . 

PROVO RIVER. 

[Drainage area, 640 square miles.] 



Date. 



Discharge. 



Maxi- 
mum. 



1904 

January 

February. . . 

March 

April 

May 

June ... 

July 

August 

September . . 

October 

November.. 
December . . 

Year. 

1898 

1897 

1895 



Sec-feet. 
290 
861 



2,153 
1,625 
326 
182 
184 
146 
190 
205 



2,153 
1,212 
2,600 
1,760 



Mini- 
mvrai. 



Sec-feet. 
196 
253 
331 
353 
461 
371 
136 
134 
80 
79 
113 
113 



79 
146 
225 
192 



Mean. 

Sec-feet. 
244 
373 
388 
486 
1,145 
1,131 
202 
149 
117 
113 
139 
149 



386 



"571 
423 



Total. 



A cre-feet. 

15,000 

21,460 

23,860 

28,920 

70,410 

67,300 

12,420 

9,162 

6,962 

6,948 

8,271 

9,162 



279,900 
279,000 
414,000 
306,400 



Run-off. 



Per 
square 
mile. 



Sec-feet. 

O.08I 

.583 

.606 

.759 

1.79 

1.77 

.316 

.233 

.183 

.177 

.217 

.233 



.604 
,60 



Depth. 



Inches. 

0.439 

.629 

.699 

.847 

2.06 

1.98 

.364 

.269 

.204 

.204 

.242 



8.20 
8.19 
12.12 
9.07 



Relation 
to rain- 
fall. 



Per cent. 

23 

24 

19 

67 

100 

347 

107 

41 

204 

15 



Rainfall. 



Inches. 

1.91 

2.64 

3.62 

1.26 

2.06 

.57 

.34 

.66 

.10 

1.39 

.00 

1.48 



16.03 

16.71 

17.76 

a 14. 63 



a Approximate. 

SPANISH FORK. 

[Drainage area, 670 square miles.] 



1904. 

January 

February... 

March 

April 

May 

June 

July.. 

August 

September.. 

October 

November.. 
December.. 

Year. 



113 


.58 


77.6 


4,771 


0.116 


0.134 


8.1 


126 


58 


79.1 


4,550 


.118 


.127 


7.4 


240 


63 


85.8 


5,276 


.128 


.148 


4.4 


229 


110 


174. 


10,350 


.260 


.290 


28.0 


415 


236 


343.0 


21,090 


.512 


.590 


25.0 


, 255 


111 


162.0 


9,640 


.242 


.270 


41.0 


121 


80 


94.6 


5,817 


.141 


.163 


39.0 


92 


67 


75.8 


4,661 


.113 


.130 


19.0 


75 


65 


68.0 


4,046 


.101 


.113 


13.0 


69 


65 


67.8 


4,169 


.101 


.116 


. 11.0 


fiQ 


49 


61 5 


3,660 
3,339 


092 


102 




77 


40 


54.3 


.081 


.093 


8.7 


415 


40 


112.0 


81,370 


.167 


2.28 


15.4 



1.66 
1.71 
3.36 
1.02 
2.33 



.85 
1.01 

.00 
1.07 



14.78 



Comparison of ttie discliarge of several streams shows marlied differences. For instance, 
during 1901 and 1902, tlie only years when complete measurements of both Parleys and 
Big Cottonwood creeks are available, the discharge of Big Cottonwood (drainage area, 48 
square miles) averaged 47,308 acre-feet, while that of Parleys, with a drainage area slightly 
greater (50 square miles), averaged only 13,303 acre-feet. Again, during 1904 the dis- 
charge of City and Emigration creeks, each having drainage areas of approximately 19 
square miles, amounted, respectively, to 12,604 and 2,332 acre-feet. Provo and Spanish 
Fork rivers also afford similar results. The drainage area of Provo River (640 square miles) 



HYDROGRAPHY. 



23 



is slightly loss than that of Spanish Fork (070 square miles), yt't the discliargc of the 
former in 1904 was more than three times that of the latter. 

It will be noticed that the flows of Spanish Fork and of Emigration Creek, streams 
which in the above comparisons figured poorly, have much in common, though their drain- 
age areas difi'er greatly. The flow of the two streams, expressed in second-feet per square 
mile of their drainage areas, averaged 0.167 for Spanish Fork and 0.169 for Emigra- 
tion Creek, which may be compared with an average of 0.746 for City Creek and 0.69 for 
Provo River. The amount of discharge, expressed in depth of inches, over the watershed is 
2.28 for Spanish Fork 2.30 for Emigration Creek, and 10.33 for City Creek. The run-off is 
approximately 15 per cent of the precipitation for Spanish Fork and Emigration Creek, 
and about 63 per cent for City Creek. 

These and other discrepancies are due to a complex set of causes, chief of which are differ- 
ences in precipitation, topography, vegetation, soils, and rocks of the several drainage areas, 
and the care that is taken to prevent fires, grazing, and destruction of timber on the water- 
sheds. Though in general the main streams in the Wasatch Mountains have many features 
in common, the valleys of some of them are narrow and steep, whil'e those of others are 
broader and more open. Some valleys are better adapted than others, by configuration 
and position, to collect and keep snow. Some of the streams head in lakes, while others do 
not. All are poorly clothed with trees, but some are less fortunate in this respect than others. 
The soil covering in general is thin, particularly on the steep slopes and in areas where the 
absence of much vegetation allows the products of rock disintegration to be washed into the 
valleys. But where the slopes are comparatively gentle and vegetation protects the accu- 
mulated rock debris, more of the precipitation is absorbed and (escaping flood discharge) 
seeps slowly into the valleys to maintain the perennial flow of the streams. Differences 
in the porosity of the bed rocks and in the character and quantity of debris in the stream 
beds, whereby greater or less amounts of water are absorbed, also greatly influence the 

amount of run-off. 

UTAH Lake. 

Utah Lake is fed from several sources, including surface streams, seepage, springs l^eneath 
the lake, and the precipitation that falls upon it. The measurable factors were determined 



tttv.T 


OU 


1889 


1890 


1891 


1892 


1893 


1894 


1895 1896 


FEcr 
4491 
90 
89 
.68 
87 
86 
85 
84.' 
83 
82 


- 




















A 




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A 


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1897 




1898 


1899 


1900 


1901 


1902 


1903 




1904 




















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Fig. 3.— Diagram showing fluctuations oi the surface of Utah Lake, 1S89-1904. 



24 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



for the period August 1903, to August, 1904, under the direction of G. L. Swendsen,o of the 
United States Reclamation Service, who found that of the total supply of 604,010 acre- 
feet only 471,140 were contributed by rainfall on the lake and by the measurable surface 
streams, leaving an unmeasured supply of 132,870 acre-feet. This considerable amount 
appears to be contributed by seepage and by springs, some of which have recently been 
found in the northwestern part of the lake. 

The surface of the lake is subject to considerable variation in elevation in consequence 
of the changing relations of evaporation, precipitation, inflow, and outflow. Fig. 3, pre- 
pared by the Reclamation Service, shows fluctuations of the surface from 1889 to 1904. 

There is a seasonal variation of 1 to 4 feet, ranging from a minimum in the late fall to a 
maximum in late spring and early summer. The diagram also shows the variation in 
the mean level of the lake. The lowest elevation shown occurred in 1903, when the lake 
was about half a foot lower than it was in 1889. Following 1889 was a period of ten years 
of relatively high water. 

JORDAIS^ RIVER. 

During the last few years anomalous conditions have existed at the outlet of Utah Lake. 
The water level of the lake has fallen so low that the normal flow has ceased, and in order to 
supply the canals in Jordan Valley it has been necessary to resort to pumping. Accord- 
ingly a pumping plant has been in operation at the head of Jordan River since August, 1902. 
(PI. IV, A.) 

The following table of discharges has been prepared by Mr. J. Fewson Smith, jr., water 
commissioner: 

Discharge of Jordan River and the canal systems in Jordan Narrows, and of Jordan River at 
pumping plant, April to October, 1904. 

[Acre-feet.] 



Month. 



North 
Jordan. 



East 
Jordan. 



City. 



South 
Jordan. 



Utah and Jordan 
Salt River at 
Lake. weir. 



Sum of 
preced- 
ing. 



Jordan 
River at 
pumping 

plant, a 



1904. 

April 

May 

June 

July 

August 

September . . 
October 



963 
2,970 
3,384 
3,233 
2,662 

753 



650 
3,036 
5,701 
5,369 
5,186 
5,280 
1,920 



452 
3,199 
3,090 
1,373 

399 



647 
5,167 
6,648 
5,407 
5,031 
5,357 
2,134 



720 
4,150 
7,878 
6,719 
7,110 
7,992 
3,367 



75 
2,911 
4,225 
3,894 
3,668 
2,767 
310 



2,092 
16,823 
27,874 
27,972 
27,318 
25,431 



222 
18,090 
25, 110 
25,210 
24,720 
23,330 
8,363 



Total. 



13,965 27,142 



,109 



30,391 



37,936 17,850 



136,; 



125,045 



Figures furnished by G. L. Swendsen. 



From these figures it appears that the gain in the flow of Jordan River between the pump- 
ing plant and the intake of the canals in Jordan Narrows, a distance of about 13 miles, April 
to October, 1904, was 11,348 acre-feet. The gain is partly supplied by seepage and partly 
by the flow of wells and springs. Between Jordan Narrows and the head of North Jordan 
canal, a distance of about 9 miles, Mr. J. Fewson Smith, jr., found that the seepage into Jor- 
dan River between May and September, 1904, amounted to 13,789 acre-feet. 



oThe writer acknowledges his indebtedness to Mr. Swendsen for many courtesies extended, both in 
the field and office, during the prosecution of the work. 



U. S. GEOLOGICAL SURVEV 



WATER-SUPPLY PAPER KO. 157 Pl. IV 



I! issi: iaea., i-mt >>t^t '.n i 



*>^^ 




^. GATE AT HEAD OF JORDAN RIVER. 




DEAD MAN'S FALLS, COTTONWOOD CANYON 



HYDROGRAPHY. 25 

No systematic data have been collected below the head of North Jordan canal, but in 
December, 1904, the following measurements were made by Mr; Caleb Tanner and the 
writer : 

Diacharge of Jordan River and tributaries between Little Cottonwood Creek ami the ford, in 
sec. i, T. 1 N.,R. 1 W., December 0-7, J90J^. 

Second-foet. 

Jordan River above mouth of Little Cottonwood Creek (il . 38 

Little Cottonwood Creek 8-14 

Flume at Taylorville roller mill 39. 

Hig Cottonwood Creek -tI-Z 

Ditch south of Mill Creek 2. 12 

Mill Creek -^ -3. 94 

Ditch, outlet of Decker Lake -* 2. 93 

Parleys Creek, north and south ditches 8. 78 

f:ighth South street ditch G. C9 

Total 203. 58 

Jordan River below North Temple Street Bridge 190. 22 190. 22 

Loss between mouth of Little Cottonwood Creek and North Temple street 13. 30 

Outlet of Hot Springs Lake 7. 64 

Sewer ditch (estimate) 7. 50 

Jordan River at ford, sec. 4, T. 1 N., R. 1 W 214.00 

Total 205. 30 205. 30 

Gain between North Temple Street Bridge and ford 8. 04 

Loss in the flow of Jordan River, instead of expected gain, is thus shown between the 
mouth of Little Cottonwood Creek and North Temple Street Bridge at the time the measure- 
ments were made, while a slight gain is shown between the bridge and the ford in sec. 4, T. 
1 N., R. 1 W. It appears that the seepage drains into the tributaries rather than directly into 
Jordan River in the area where the tributary streams are numerous and that farther north, 
where there are fewer tributaries, a small amount of seepage drains directly into the river. 
How far these figures represent conditions the year round remains to be determined. 

GREAT SALT LAKE. 

Except during a lapse from 1893 to 1896, instrumental records of the surface fluctua- 
tion of Great Salt Lake have been kept since 1875, and there is evidence less exact dating 
back to the survey of the lake by Stansbury in 1849-50. When that survey was made the 
level of the lake was extremely low, and since then it has varied considerably. In 1869 
the water surface was approximately 11 feet higher than it was in 1850; a comparatively 
low stage was reached in 1873, after which the lake rose about 4 feet to a maxinumi in 
1876, about equal to that attained in 1869. In 1883 the lake was about 7 feet below the 
maximum; then it rose 4 feet until 1886, since when it has gradually fallen until now it is 
at an extremely low stage, about 15 feet lower than the maxima of 1869 and 1876. Fig, 
4 illustrates the changes since 1875. 

Besides the irregular fluctuations there is a regular annual variation ranging between 1 
and 2 feet, the maximum occurring in June and the minimum in the winter This annual 
variation is due to the changing relations of precipitation, inflow, and evaporation, high 
water occurring after the spring floods, and low water during the season of fe(>ble stream di.s- 
charge and after the period of excessive evaporation. The irregular variation of the 
past can be accounted for chiefly by changes in rainfall, the earlier nuixima being associ- 
ated with unusually large amounts of precipitation. The gradual decrease of late years 
in tlie volume of the lake, after allowing for recent dry seasons, is apparently due to 
largely increased irrigation, by which the inflow of surface streams has been checked 



26 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



through diversion into ditches. Because of the considerable evaporation and transpira- 
tion incident to such use of the water, only a small per cent of the run-off reaches the 











































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lake, and with the spread of irrigation it may be expected that this cause will increasingly 
tend to keep the lake level at a low stage. 



SOURCES OF GROUND WATER. 27 

UNDERGROUND WATER. 

GENEKALi CONDITIONS. 

SOURCE. 

The underground water supply in the valleys of Utah Lake and Jordan River, as is well 
known, is maintained by the snow and rain that fall on their drainage areas. In con.sid- 
ering the sources of the supply, the precipitation tributary to Utah Lake and Jordan River 
can conveniently be divided into that on the mountains and that on the main valley. 

It has been stated that the actual precipitation in the mountains probably exceeds the 
amount shown by the recorded data. Moreover, neither the rainfall nor the snowfall is 
evenly distributed. The precipitation is greater in the northern than in the southern half 
of the area under consideration, and in contiguous localities there are differences due to 
varying topographic conditions. More precipitation is likely to occur in the vicinity of the 
higher peaks, and in the mountain recesses that are well protected from the sun large quan- 
tities of snow linger long after the general mantle has disappeared. 

Of the total precipitation on the mountains, part is evaporated, part joins the run-ofl", and 
part becomes underground water. Evaporation occurs either directly — from snow, from 
a free surface of water, and from water contained in soils and brought to the surface by 
capillary action — or indirectly by transpiration through the growth of plants. Of the por- 
tion which joins the run-off part runs directly out of the mountains, part flows to small 
lakes at the head of Big Cottonwood Creek and Provo River, and part is absorbed by the 
soil and rocks over which the streams flow and joins the subterranean store. A final portion 
of the precipitation on the mountains becomes underground water directly by absorption 
by the surface on which the rainfall occurs. Part of this underground water reaches the 
surface again by capillary action in the soils and by the life activity of plants and is finally 
evaporated; another part after remaining underground a shorter or longer time reaches 
the surface again by springs and seepage, and, joining the run-off little by little, maintains the 
perennial flow of the streams; another part joins the more permanent supply of underground 
water. It is impossible, because of the complexity of the subject and the lack of data, to 
state the amount of water which annually replenishes this more permanent supply of 
underground water, but the quantity is equivalent to the precipitation minus the run-off 
and the amount evaporated. From the incomplete facts at hand it appears that the run-off, 
measured at the mouths of the canyons, although varying greatly, approximates 50 per cent 
of the precipitation, but the total evaporation is unknown. Although exact figures repre- 
resenting the amount evaporated can not be obtained, yet experiments on evaporation from 
snow, soils, and vegetation in the mountain areas would afford valuable data. 

The amount of precipitation in the valley is better known, and the figures for Salt Lake 
City and Provo are typical. Here, as in the mountains, part of the precipitation joins the 
run-off, part is evaporated, and part becomes underground water; but there are practi- 
cally no measurements of these different quantities. Direct run-off of the precipitation 
on the valley is comparatively small, owing to the open nature of the country and to the 
fact that no great accumulations of snow occur, and the seepage run-off probably consti- 
tutes the main amount. Evaporation from soils and vegetation dissipates probably the 
largest part of the rain that falls on the valley, especially during the summer. The increase 
of the more permanent underground water supply due to the rainfall on the valley is con- 
sequently small. A basis for judgment is furnished by comparing the condition of the 
valley east and west of Jordan River. Precipitation is perhaps slightly less in the western 
part of the valley, but the difference is not enough to cause the marked contrast. The scarc- 
ity of ground water within easy reach of the surface in the western part of the valley, com- 
pared with the abundance easily accessible in the eastern part, implies that the rainfall on 
the valley contributes a proportionally small amount to the store of underground water. 
Existing conditions are due to the fact that on the west only a few feeble and generally 
intermittent streams are tributary to the valley, whereas on the east a number of large 
perennial streams flow from the Wasatch Mountains, supplying water that is distributed 



28 UNDERGROUND WATER IN VALLEYS OF UTAH. 

over the valley by canals. Seepage from these streams is the main source of underground 
supply in the valleys. 

The amount of water contributed to the valleys by streams from the Wasatch Mountains 
is capable of rough numerical statement. The drainage area in these mountains tributary 
to Jordan Valley is approximately 220 square miles, and measurements of five creeks in that 
region, given in the section devoted to hydrography, show an average flow of 0.66 second- 
foot per square mile of watershed. This amount is equivalent to a stream discharging 145 
second-feet, or a total amount approximating 105,000 acre-feet a year. The average of 
measurements of Provo River and Spanish Fork in Utah Lake Valley gives a flow of 0.43 
second-foot per square mile of drainage area, which, assuming the flow to be derived from 
rainfall on a watershed of about 1,670 square miles, is equivalent to a stream discharging 718 
second-feet, amounting to 520,000 acre-feet a year. 

Of this amount of water annually contributed by streams to the valleys of Utah Lake 
and Jordan River, part permanently runs off and is added to the supply of Great Salt Lake 
by Jordan River. This quantity has not yet been systematically measured, but it is esti- 
mated to average about 200 second-feet. The residue either evaporates, directly and indi- 
rectly, or becomes underground water. Unfortunately, no figures are available whereby 
the amount lost by evaporation can be estimated, so that the annual replenishment of the 
underground supply is unknown. Only the crude statement can now be made that, in the 
presence of influences sufficient to cause an evaporation of 60 inches a year from a free body 
of water, the amount which is not thus lost from a supply of somewhat more than 600 
second-feet joins the underground store. 

Seepage measurements which have been made at different times in both valleys from 
creeks and ditches offer concrete demonstrations of the manner in which the underground 
supply is maintained. Only a few such measurements have been made in Utah Lake Valley, 
but it has been shown that in IJ miles the Timpanogas canal lost slightly more than 25 per 
cent of the water taken in at its head.a Another set of measurements has been made on 
Provo River. The discharge a short distance above the mouth of the canyon was found to 
be 175.04 second-feet; at a station a mile west of Provo the river was dry, while the 
sum of several intermediate diversions amounted to 186.22 second-feet. The difference — 
11.18 second-feet — represents the return seepage from the various canals. & In the valleys 
of creeks tributary to Jordan River more measurements have been made, of which those in 
Big Cottonwood and Mill valleys are typical. In Big Cottonwood Creek Valley Mr. E. R. 
Morgan selected for measurement two sections of the creek on which different conditions exist. 
In the upper section, immediately below the mouth of the canyon, the bed of the stream 
is composed of large loose bowlders resting on coarse gravel, and the land on either side is 
covered with comparatively scanty vegetation. In the lower section, below the head of 
Green ditch, the bed of the creek is comparatively smooth, and the land on both sides is irri- 
gated and covered with abundant vegetation The loss in the first section, in a distance of 
2^ miles, was 7.36 second-feet, a percentage of 22 6, while in the second section, also 2| 
miles long, the loss was only 0.30 second-feet, a percentage of 2.4.c In Mill Creek Valley 
Mr. Morgan also made measurements in two sections where different conditions exist. In 
one section, 2 miles long, he found a loss of 22.7 per cent; in the other, three-quarters of a 
mile long, he found a loss of 3.6 per cent.d 

While seepage from the flow of the creeks and canals furnishes the chief supply of under- 
ground water to the valleys of Utah Lake and Jordan River, other sources are the underflow 
of the creeks at the mouths of the canyons, springs from bed rock, seepage at the base of 
the mountains, and the small addition, already mentioned, derived from rainfall on the valley. 
The underflow of the creeks at the mouths of the canyons is an important source, but the 
amount thus contributed is unknown. The quantity equals the remainder after subtract- 
ing the sum of run-off and evaporation from the precipitation, of which factors only the 
run-off is established, the precipitation being only approximately and the evaporation not 
at all known. The amount of the underflow can be directly determined, however, by a series 



a Bull. U. S. Dept. Agric. No. 124, Office Expt. Stations, 1903, p. 123. 
6 Ibid., p. 126. 

c Morgan, E. R., Irrigation in Mountain water district, Salt Lake County, Utah: Bull. U. S. Dept. 
Agric. No. 133, Office Expt. Stations, 1903, pp. 60-61. 
d Ibid., pp. 44-45. 



U. S. GEOLOGICAL SUftvSv 



WATER-SUPPLY PAPER NO. 15? PL. V 



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EXPLANATION 




W 


Soil 

Clay 

Sand 

Dark clay 

Coarse sand 

Sandy clay 

Fine sand 
Clay 

Quicksand 

Sand and 

gravel 
Hard clay 

Gravel 
Hardpan 
Clay and 
gravel 

Scale 

60 loofoet 


'~^"£" 








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1 



WELL SECTIONS. 



No. 1, Oregon Short Line well at Kaysville; No. 2, Southern Pacific Company's well at Strongs Point; 
Nos. 3-24, location shown on Pis VII and VIII. 



SOURCE AND DTSTRrBUTION. 29 

of measurements which should be made in estinmt ing the feasibility of constructing sub- 
surface dams. The amount of water cont'-ibuted to the valleys from bed-rock sources is 
also important. A remarkable series of thermal springs is a.ssociated with the great fault 
at the western base of the Wasatch Mountains. These occur at intervals along the entire 
extent of the range, and other warm springs, which may also })e connected with faults, are 
located within the area under consideration. Association with faults suggests a deep- 
seated origin, which accounts for the high temperature of the water. The last source of the 
valley water supply to be mentioned is the comparatively small amount which is derived 
by seepage from the base of the mountains from areas that are not drained by creeks. 

DISTRIBUTION OF UNDERGROUND WATER. 

From the outline of the geology given on pages 7-13 it will be seen that the valleys of Utah 
Lake and Jordan River are occupied by a considerable but unknown thickness of gravel, 
sand, and clay derived from the disintegration of the adjacent mountains and deposited in 
the valley under alternating subaerial and lacustrine conditions. In general, the deposits 
are arranged in broad, sheet-like accumulations, the coarser-textured materials abounding 
adjacent to the highlands and the finer debris preponderating farther out. The beds lie 
practically flat in the center of the basins, but are inclined slightly away from their source, 
the attitude of deposition being practically unaltered. Conditions of deposition, however, 
were so varied that over large parts of the area considered the deposits are not widely 
uniform. For instance, while clay was being laid down in one place sand was accumulating 
in an adjacent area and at their border the two deposits were merged. Consequently the 
arrangement of the beds is broadly lenticular, as is illustrated by the well records (PI. V). 
No two records are exactly alike, and in most cases it is impossible to correlate deposits 
in the different sections. Beds of clay are most widely distributed, but the more localized 
accumulations of sand and gravel, which are the most important reservoirs of underground 
water, are irregularly distributed. 

Underground water derived from the sources stated above occupies the spaces between 
the solid particles of the clay, sand, and gravel which constitute the valley filling. In 
general, these deposits are saturated below the horizon which marks the surface of ground 
water. The position of this surface varies, depending on the supply, on the ajnount used 
or the intensity of evaporation, and on the character and slope of the sediments. The water 
is seldom stagnant, but tends to flow with extreme slowness from a higher to a lower level, 
the chief factors in the movement being the number and size of the interstitial spaces in 
the deposits and the pressure gradient due to gravity. The highest velocity of ground 
water ever determined is about 100 feet in twenty-four hours, but the ordinary velocity is 
mucli less than this, common rates in sand being between 2 and 50 feet a day. 

The fluctuation of the surface of ground water is considerable. Since the chief replen- 
ishment of the supply occurs when the creeks discharge the most and when the irrigation 
canals are in full operation, ground water occurs nearer the surface in summer than in 
winter. Conditions in different areas cause a varied annual range, but 10 feet is connnon 
and 15 feet is not infrequent. In addition to the annual fluctuation a cumulative change 
is in progress, the ground-water surface being graduall}^ raised in the lower parts of the 
valley in consequence of irrigation and the custom of allowing artesian wells to flow uncetis- 
ingly, leading to swampy conditions in the valley bottom. Details regarding these changes 
arc given on subsequent pages. 

PI. VI illustrates the approximate average depths at which ground water occurs in the 
valleys of Utah Lake and Jordan River. The boundaries between the did'erent areas 
fluctuate andean not accurately be determined. A narrow belt contiguous to the base of 
the mountains is left blank on the map because of the varying and often unknown condi- 
tions that exist there, owing to seepage and the irregular distribution of water in the 
adjacent bed rocks. In the absence of topographic maps the position of the water table 
can not be shown by contours. 

Below the surface of ground water the saturated beds contain varying amounts, depend- 
ing on the character of the deposits. Coarse-textured gravel and sand, having a greater 
porosity than fine-textured clay, hold and transmit relatively more water. Beds of sand 
and gravel therefore constitute the chief underground reservoii-s. Typical illustrations of 
the distribution of sand and gravel are shown in PI. V. In sinking wells in this region, beds 



30 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



of sand and gravel, ranging from a few inches to a hundred feet or more and separated by- 
varying thicknesses of clay, are encountered, water being commonly found in each porous 
deposit. Because of the prevailing inclination of the deposits away from the mountains, 
and of the presence of relatively impervious beds of clay above more porous sand and 
gravel, the contained water is under pressure. In the lowland areas this pressure is suffi- 
cient to cause the deep-seated water, when it is reached in a well, to rise and flow at the 
surface, and consequently artesian water is an important source of supply. Above the 
lowlands, where the surface elevation is too great for a flow to occur at the surface, the 
water rises in deep wells to a greater or less height according to the amount of pressure. 

aTTALITY OF UNDERGROUND WATER. 

The accompanying analyses, gathered from a number of sources and reduced to common 
terms, illustrate the character of the water in the valleys of Utah Lake and Jordan River. 

of water from streams and springs in valleys of Utah Lake and Jordan River.O' 
[Parts per million.] 



No. 


Source and date. 


Ca. 


Mg. 


Na. 


K. 


AI2O3 


FezOa 


Si02. 


SO<. 


HCO3. 


CO2. 


CI. 


Total. 




CREEKS. 












1 




















1 


City, Dee., 1882. 


55.3 


18.9 


2.6 


24.3 


2.0 


19.9 


7.3 




95.1 


19.5 


244.9 


2 


Red Butte, 
Dec., 1882 


88.8 


31.3 


• 25.6 


Trace 


3.3 


35.2 


100.6 




108.8 


22.9 


416.5 


3 


Emigration, 
Dec, 1882 


101.0 


31.6 


18.1 


9.9 


2.6 


24.4 


126.2 




102.7 


28.6 


445.1 


4 


Parleys, Dec., 
1882 


85.1 


22.5 


31.5 


2.6 


1.8 


27.2 


56.5 




122.1 


19.7 


369.0 


5 


Big Cotton- 
wood, Oct. ,1884 


48.1 


18.9 


Trace. 


8.6 


1.6 


12.6 


42.1 




63.6 


7.9 


203.4 


6 


Little Cotton- 
wood, Oct., 1884 


17.5 


8.2 


5.9 


1.7 


1.3 


39.9 


12.3 




32.2 


2.8 


' 121.8 


7 


Dry Cotton- 
wood 


17.0 
45.0 


27.0 
24.0 


15.0 
4.0 


14.0 
10.0 






34.0 
42.0 


121.0 
145.0 




14.0 
Trace. 


242.0 


8 


American Fork . 






270.0 


9 


Payson 


12.0 


17.0 


22.0 


3.0 






32.0 


121.0 


14.0 




221.0 


10 


Santaquin 


12.0 


31.0 


31.0 


5.0 






33.0 


212.0 


14.0 




338.0 


11 


Currant 

Warm 


47.0 
114.0 


54.0 

48.0 


89.0 
381.0 


44.0 
92.0 






115.0 
114.0 


181.0 
333.0 


15.0 
28.0 


211.0 
703.0 


756.0 


1? 






1,813.0 




RIVERS. 
























13 


Provo 


51.0 
68.0 


29.0 
36.0 


28.0 
46.0 


22.0 
17.0 






44.0 
64.0 


205.0 
277.0 




28.0 
28.0 


397.0 


14 


Spanish Fork.. . 
Jordan: 


1 


536.0 


























15 


Utah Lake 
(outlet), 1899. 


67.6 


13.8 


233.7 


2.0 






236.7 




23.7 


316.5 


894.0 


16 


Salt Lake Citv 
(near), 1899. 

WARM SPRINGS. 


111.8 


13.7 


251.1 








334.5 




Trace 


378.9 


1,090.0 


17 


Salt Lake City, 
Oct., 1881... 


535.2 


138.4 


3,039.0 


178.0 


0.7 


21.3 


787.5 





442.9 


4,968.0 


10,284.0 


18 


Beck's (hot).. 


694.3 


109.5 


3,754.9 


196.9 


9-0| 


31.5 


840.5 




204.5 


6,743.8 


12,584.9 


19 


Sandy (8mi. s.). 
Mar. 1882 

UTAH LAKE. 


141.5 


27.7 


405.0 


55.0 


5.1 


50.5 


53.8 




272.7 


635.6 


1,658.0 


?n 


1883 


55.8 
67.0 


18.6 
86.0 


17.7 
230.0 


2.0 
22.0 




10.0 
28.0 


130. 6 

378.0 194.0 


60.9 
11.0 


12.4 


308.0 


■^l 


1904 




337.0 1,353.0 

















a Authorities.— Nos. 1-5, 17, 19, Kingsbury, J. T. Nos. 6-14, Soil survey of the Provo area, Utah: 
Bureau of Soils U. S. Dep-t. Agric, 1904, p. 22. Nos. 15, 20, and 21, Cameron, F. K. Water of Utah 
Lake: Jour. Am. Chem. Soc, vol. 37, No. 2, 1905. No. 16, ibid.. Kept. No. 64 U. S. Dept. Agric. No. 
18, Riggs,R.B., Bull. U.S.Geol. Survey No. 42, 1887, p. 148. No. 20, Clarke, F.W. No. 21, Brown, R.E. 



. S. GEOLOaiCAL SURVEY 



WATER-SUPPLY PAPER NO. 157 PL. 




EXPLANATION 



] Area in wh/'c/i grouna/ wafer //es 
\ wfh/r? /Ofeefoffhe surfcyce 



\ Area in w/iic/i groi/nc/ wo/er //es 

\ befwee/? /Oanc/ 50 feet b e/ofv 

the surface 



\Area inivhici) grounc/wa/er/ies 
surface 

Base of mountains, approximofe pos/fon 
offfeBonnei//ffe sfore f/ne 



SKETCH MAP SHOWING DEPTH TO GROUND WATER IN THE VALLEYS OF UTAH LAKE AND JORDAN RIVER. 



QUALITY OF UNDERGROUND WATER. 81 

The average of analyses of 12 streams « coming from the Wasatch Mountains shows a 
total solid content of 319 parts per million, ranging from 122 to 536, the varying character 
of the water being duo to differences in the rocks of the respective watersheds. Examina- 
tion of these analyses shows that calcium is usually the most abundant base, with magne- 
sium a poor second, while sodium and potassium generally are much less plentiful and 
vary in relative amounts. Among the acid radicals, carbonic commonly preponderates, 
being often several times more abundant than the others; sulphuric ranks next, and in a 
few streams is important, while chlorine is generally of minor occurrence. Little Cotton- 
wood Creek ranks first, having only 121.8 parts per million of dissolved solids. It flows 
for most of its course through granitic rock and therefore contains but little calcium car- 
bonate. The total solids in Big Cottonwood Creek water are also low and relatively little 
lime is present because a large part of the drainage is over silicious rocks. The great 
abundance of limestone on most of the watersheds accounts for the abundance of calcium 
carbonate. Red Butte, Emigration, and Parleys creeks make a relatively poor showing, 
the sulphates being especially abundant, because these streams flow over Permo-Carbon- 
iferous and Mesozoic rocks containing more or less gypsiferous matter. Provo River and 
Spanish Fork drain large areas occupied by a variety of rocks, among which limestone is 
prominent, and the analyses show rather high amounts of total solids, the carbonates 
being particularly abundant. Currant and Warm creeks are exceptional. The unusual 
amount of sodium chloride present in Currant Creek is derived from salt deposits above 
Nephi. Warm Creek rises in the springs west of Goshen, and the character of its water, 
like that of similar springs in this area, is due to unusual conditions. 

The few analyses of the thermal springs in the area under consideration show the presence 
of abundant dissolved salts, of which the chlorides are the most plentiful, though consid- 
erable quantities of sulphates and carbonates are also present. Sodium is several times 
more abundant than any other base, calcium ranks second, and magnesium and potassium 
are present in small amounts. Some of the hot springs contain considerable hydrogen 
sulphide. Most, if not all, of these springs are associated with faults and have a deep- 
seated origin, to which their temperature and composition are due. The mineral matter 
is leached from the deposits through which the waters pass, much of the salt content 
being probably derived from old lake beds. 

Analyses of water from flowing wells are similar to those of surface streams. Different 
wells give different results, the quality of the water varying with the source and the nature 
of the deposits passed through underground. Analyses from the "Murray" and "Ger- 
mania" wells show an unusually small content of total solids, while those from the wells 
of the Utah Sugar Company at Lehi and near Provo show amounts above the average. 
In the area contiguous to Great Salt Lake the well water contains considerable salt, but 
no analyses were obtained. In general the water from flowing wells is of admirable 
quality and often forms a marked contrast to the supply from shallow wells. 

a Omitting Currant and Warm creeks, which are exceptional. 



32 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



Analyses of water from wells, etc., in valleys of Utah Lake and Jordan River. f' 

[Parts per million.] 



No, 



Source and date. 



Mill Pond at Lehi, July ,1895 

Artesian well,Murray Plant; 
Am. Smelting and Refin- 
ing Co 

Artesian well, Germania 
Plant, Am. Smelting and 
Refining Co 

U. S. Mining Co. well, Bing- 
ham Junction, Aug., 1902 

U. S. Mining Co. well. West 
Jordan, Aug., 1902 

Wm. Cooper's well, Bing- 
ham Junction 

Beet-cutting station, Utah 
Sugar Co.well,near Provo. 
Jan., 1899 '. 

Artesian well, Utah Sugar 
Co., Lehi, Jan., 1899 

R. G. W. Rwy. well, Spring- 
ville, May, 1901 

R. G.W. Rwy.well, Goshen, 
May, 1901 



Ca. 



Mg. 



Na. 



AI2 
O3. 
Fe2 
O3. 



16.0 



1 

2.4 
1 
1.2 

5 
Tr. 

4 
90 



SiOz. 



14 

9.7 
14 
13 
16 

58 
12 
18 
80 



SO4 



dl96 

dl4 

dl2 
d50 



dl6 



154 
41 

47 



CO3. 



?>135 

42 

64 

56 

c30 

66 

C180 
c91 
120 

127 



CI. 



68 



Na2 
CO3 
K2 
CO3. 



124 



Na2 
SO4 
K2 
SO4. 



Tr. 

6.8 
27 

44 
45 

116 



Na 

CI 

KCl, 



152 



28 
87 
58 
87 

103 

287 



Total 
sol- 
ids. 



114 

140 
290 
232 

284 

056 

648 



aAuTHORiTiES.— Nos. 22, 28, and 29, Dearborn laboratories. Nos. 25 and 26, Converse, W. A. No. 27, 
J. H. Parsons Chemical Co. Nos. 30 and 31, De Bernard, J. H. 
b From MgCOs. 
c From CaCOs and MgC03. 
d From CaSO^. 



No analyses of ground water obtained from shallow wells are available, but the general 
character of such water is known. In the upland areas above the canals the water from 
shallow wells is much like that commonly obtained throughout the region in deeper ones; 
it contains a moderate amount of dissolved salts, largely calcium carbonate, and is usually 
of good quality. But in the lowlands the surface water is quite different, generally con- 
taining considerable dissolved salts, among which alkalies are abundant. Where ground 
water lies within the scope of capillary attraction from the surface, evaporation causes the 
mineral matter which is held in solution to accumulate, and in this manner the soil becomes 
tainted with alkali. Consequently the water from surface wells in the lowlands is charac- 
teristically rich in dissolved salts. 

Abnormal conditions prevail locally in the vicinity of the smelters in Jordan Valley 
south of Salt Lake City. Smelter smoke has lately become a nuisance to farmers by 
injuring crops and animals in the path of prevailing winds. Sulphur dioxide is the 
most abundant deleterious substance contained in the smoke, and to a minor extent locally 
finds its way into the water supply. Occasionally also ground water may become poisoned 
from accumulations of flue dust containing copper and arsenic, a 

Natural gas occurs in a number of water wells in the area under consideration. Well 
drivers report the common presence of vegetable matter, chiefly fragments of wood, at 
different depths in many localities. This was entombed in the old lake deposits, and its 
decomposition may account for the origin of the gas. Though gas occurs in numerous 
wells it has been found in quantity in only a few localities, the greatest development occur- 
ing near the shore of Great Salt Lake, about 12 miles north of Salt Lake City, b Here 
several wells were drilled averaging about 500 feet in depth; and from September, 1895, 

a Widtsoe, J. A., Relation of smelter smoke to Utah agriculture: Bull. Agricultural College of Utah 
No. 88, 1903. 
b Richardson, G. B., Natural gas near Salt Lake City: Bull. U. S. Geol. Survey l<io. 260, 1905, p. 480. 



QUALITY OF UNDERGROUND WATER. 83 

to March, 1897, Salt Lake Cit}^ was suppiicd with natural ga.s from this sourcp, tho total 
yield l)oing approxiniateh' 1,5(),00(),0(X) cuhic foot. But tho supply finally hocamo insuffi- 
cient and the field was abandoned. Gas continues to ho found in various parts of the valley 
and p(xssil)ly other fields similar to that north of Salt Lake City may yet be found; but 
there is little reason for expecting much better results than already obtained and it is 
impossible to predict the localities where such supplies may be found. 

The water of Utah Lake represents the varied sources of its supply; part is derived 
directly from surface streams, another part from seepage, still another portion from springs, 
and the whole is concentrated by evaporation. The analysis by the Bureau of Soils on 
page 30 shows the present condition of the water. Sodium predominates, magnesium and 
calcium are subordinate, and the corresponding salts are principally sulphates and chlorides. 
Comparison with an analysis of Utah Lake by F.W.Clarke twenty-one years earlier affords 
interesting data." The total solids have increased from 308 to 1,353 parts per million, 
and the character of the water has changed from a preponderating sulphate solution to 
one containing large amounts of chlorides; the sodium has increased remarkably and 
magnesium is now in excess of calcium. These changes appear to be mainly due to man's 
occupancy of the region. The streams have been diverted for irrigation and an increasing 
supply has reached the lake as seepage after passing through the alkaline soils of the low- 
lands. Evaporation in the shallow lake also has tended to concentrate its waters. 

The composition of the water of Great Salt Lake has been the subject of much investi- 
gation, and a list of the more important analyses is given on page 34. The lake receives 
the drainage of an enormous area, but by far the greater part of its supply is derived from 
the Wasatch Mountains, from Bear, Weber, arwi Jordan rivers. The mineral content of 
Great Salt Lake is the result of the concentration of a vast body of water during a long 
period of time, in which Lake Bonneville has given place by evaporation to tho present 
lake. Groat Salt Lake is shallow, and the seasonal and annual fluctuations in its level 
cause considerable difTerences in volume, with consequent changes in composition of the 
water. These changes are indicated by the increase of salinity from 13 per cent in 1873 
to about 24 per cent in 1892. 

In August, 1892, the water of Great Salt Lake contained 238 parts per thousand of 
total solids, consisting of predominating sodium and smaller amounts of magnesium, potas- 
sium, and calcium, in the order named, the corresponding salts being chlorides and sul- 
phates. The w^ater of the lake is thus a concentrated brine, and in the winter months 
the point of saturation for sodium sulphate is actually reached and crystals of mirabilite b 
are deposited. The critical point for calcium carbonate is passed, so that, in spite of its 
abundance in the waters that supply the lake, none has been found in it. Apparently 
calcium carbonate is precipitated soon after entering the dense body of water. ' 



aCameron, F. K., Jour. Am. Chem. Soc. vol. .'37, 1905, p. 113. 
ftTalmagc, J. E., "Great Salt Lake, Present and Past," 1900, p. 64. 



IRR 157—06- 



34 



UTsTDERGEOUND WATER IN VALLEYS OF UTAH. 



Analyses of water of Great Salt Lake, a 
[Parts per thousand.] 



Analyst and date. 



Gale, L. D., 1850. 

Allen, O. D., sum- 
mer, 1869 



Bassett, H., Aug., 
1873 :-. 



Talmage, J. E.: 

Dec, 1885 

Aug., 1889 

Waller, E., Aug., 
1892 



Ca. 



Trace. 



0.2 



Mg. 



0.6 
3.8 
3.0 

2.9 
5.1 



Na. 



85.3 
49.6 
38.3 

58.2 
65.3 



2. 844 75. 825 



K. 


SO4. 


CI. 


B2O3. 


P2O5. 


Total. 


2.4 
9.9 

1.9 
2.1 

3. 925 


12.4 
9.9 

8.8 

13.1 
11.7 

14. 964 


124.5 
84.0 
73.6 

90.7 
110.5 

128. 278 






222.8 
149.9 
134.2 

167.2 
195.5 

b238. 12 


Trace. 


Trace. 










Trace. 





Specific 
gravity 



1.170 
1.111 
1.102 

1.122 
1.157 

1.156 



n Waller, E., Water of Great Salt Lake: School of Mines Quart., vol. 14, 1893, p. 59. 
b By evaporation, duplicate test gave 237. 93. 

Too little care is given to the sanitary character of the waters in the valleys of Utah 
Lake and Jordan River. The mountain streams are a source of excellent purity, yet they 
are liable to contamination. General supervision of the watersheds of the creeks that sup- 
ply Salt Lake City is maintained by the municipality, especially on City Creek, but else- 
where few precautions are taken to safeguard the supply. Commonly the character of 
water obtained from the deep wells is of good quality, as is also that of surface wells in 
the thinly settled uplands adjacent to the base of the mountains. But surface water gen- 
erally, especially in the thickly settled lowlands, where, moreover, the mineral content is 
high, is undesirable for domestic use because of its liability to contamination. 

Salt Lake and Provo are the only cities in the area that have sewer systems. The 
Provo sewer discharges through an open ditch into Utah Lake, and thereby pollutes that 
body of. water. Salt Lake City's sewage is well disposed of on a ''sewer farm" below 
Hot Springs Lake, and the surplus enters Jordan River near its mouth. Elsewhere no 
systematic sanitary precautions are taken, and locally conditions are bad, with consequent 
frequent typhoid fever epidemics. 

It can not be too strongly impressed upon inhabitants of country districts that the wel- 
fare of the community is intimately concerned with preserving the water supply uncon- 
taminated, and in this connection it may be of service to reproduce a section from the ninth 
annual report of the Massachusetts State board of health : a, 

There are a fev^^ points to he borne in mind with reference to vv^ater supply, drainage of houses, and 
sewerage, which have been suggested by the examination of the board in this State, and may properly 
be summarized here. 

1. The privy system, so common throughout the State, by which filth is stored up to pollute the air, 
soil, and water near dwellings, should in all cases be abolished. 

2. Cesspools, unless extraordinary precautions be taken as to ventilation and prevention of pollu- 
tion of soil and air, are little better, and should be given up for something less objectionable as soon as 
practicable. 

3. Wells can not be depended on for supplies of wholesome water unless they are thoroughly guarded 
from sources of surface and subsoil pollution. Some of the foulest well water examined by the board 
has been clear, sparkling, ahd of not unpleasant taste. 

4. Where wells have already been polluted and it is not practicable to dig new deep wells remote 
from sources of contamination or to introduce pure public water supplies, the storage of rain water, 
properly filtered, is a satisfactory method of procedure. 

5. In small towns where public water supplies have not been introduced, and, indeed, wherever water- 
closets are not used, some method of frequent removal and disinfection with earth or ashes should be 
adopted in place of privies, by which it should be impossible for the filth to soak into the soil or escape 
into the air. Cemented vaults are not always to be depended upon, as their walls crack from frost or 
through settling of the ground, and they thus sometimes become sources of pollution of wells, besides 
contaminating the air. Nor is the fact of a privy being on a downward slope from the well a suflficient 
safeguard, for even then the direction of the subsoil drainage may be toward the well. 



o Rafter, G. W., and Baker, M. N., Sewage Disposal in the United States,1894, p. 40. 



QUALITY OF UNDERGROUND WATER. 35 

6. Earth closets, with proper care, may be satisfactorily adopted, l)Ut the earth, after having been 
once used, should be placed upon the land, not stored within doors and dried to be again used, for in 
the process of drying there are emanations from it which are, perhaps, not less dangerous from the fact 
of their being imperceptible l)y the unaided senses or through chemical examination. With earth clos- 
ets a plan similar to that in use at the I'ittsfield Hospital " may well be used for the chaml)er slops, 
and the kitchen waste may be utilized (with the chamber slops too, if desired) in the manner used by 
Mr. Field and Colonel Waring. * * * Less intricate methods are used in scattered dwellings, but 
with the effect of having the slop water absorbed by the ground and taken up by vegetation so far 
from the house as not to involve a nuisance or danger to health. 

7. Where water supplies, water-closets, etc., are introduced, sewers should follow immediately in 
most kinds of soil. Cesspools .should not be used, unless with extraordinary precautions; ])ut wiih a 
few hundred feet square of lawn the irrigation system by agricultural drain pipes is to be recon\- 
mended, whereby the filth is at once taken up by the roots of grass. In all cases, of course, with or 
without cesspools, there should be thorough ventilation of the system of house drainage, with discon- 
nection from the main outlet drain liy means of either a ventilating pipe or rain-water spout between the 
sewer trap and the house, and whose openings at the top should be only at points remote from win- 
dows and chimney tops. 

On the whole, a thoroughly satisfactory arrangement of this kind, if properly looked after, is in 
many respects to be preferred to connecting with public sewers. 

RECOVERY OF TJNDERGROTJND WATER. 

A crude estimate of the amount of underground water in the valleys of Utah Lake and 
Jordan River might be made, based on an assumed thickness and porosity of the unconsoli- 
dated sediments, and the result would be many cubic miles, yet the figures would be value- 
less. The important fact is the amount of available water that can be recovered econom- 
ically; but, unfortunately, this too, because of lack of detailed knowledge concerning the 
distribution and thickness of the beds of sand and gravel which constitute the reservoirs, 
can not be determined. Though definite figures are not available, the general fact is well 
known that the lowlands are amply supplied with underground water within easy reach of 
the surface and that on the highlands the underground supply is 'relatively small. 

Underground water becomes available for use both naturally and artificially. It reaches 
the surface again naturally in springs and by seepage into drainageways, and is commonly 
recovered artificially by means of wells, though occasionally tunnels and subsurface dams 
prove efiicacious. Wells are the main recourse in the area under consideration, and they 
can be conveniently grouped into two classes, flowing and nonflowing. 

The areas in which flowing wells are obtained in the valleys of Utah Lake and Jordan 
River are shown on Pis. VIII and IX, and the list of wells, together with the descriptions of 
the different localities, gives detailed information concerning the occurrence of artesian 
water. 

The date when the first flowing well was put down has not been ascertained, but it 
appears to have been about 1878. Since then many have been sunk, and the limits of the 
areas in which flows can be obtained have been determined with fair accuracy by experi- 
ment. The map shows that flowing wells exist only in the lower portions of the valley, 
the area of flows corresponding closely with that in which ground water lies within 10 feet 
of the surface. Higher up on the benches the elevation is too great to obtain flows. 

Locally, flowing wells may be obtained at a depth of less than 50 feet, but generally they 
range between 100 and 400 feet, while the few that have been sunk to 1,000 feet and more 
encountered water under pressure in the successive beds of sand and gravel. As many as 
25 distinct water horizons from which flows at the surface were obtained are reported in 
the Rudy well, .sec. 6, T. 1 N., R. 1 W. The wells are usually 2 inches in diameter, though 
occasionally the .shallower ones are only 1 inch, while the deeper ones are 4 and 6 inches. 
In yield the wells vary considerably, according to location, depth, and size of pipe. The 
greatest flow measured was that in the Harry Gammon well, sec. 7, T. 6 S., R. 2 E., whicli 
supplies about 266 gallons a minute from a 3-inch pipe. A number of wells flow less than 
1 gallon a minute, though a common yield is between 10 and 60 gallons. The pressure is 
comparatively low, the highest measurements obtained being only 151 pounds per square 



o Cottage Hospitals: Ninth Ann. Rept. Mass. State Board of Health, pp. 83-95. 



36 UNDERGROUND WATER IN VALLEYS OF UTAH. 

inch, and generally the greatest pressures are little more than sufficient to raise the water 
into railroad tanks. 

Temperature measurements of the water from flowing wells afford some data bearing on 
the downward increment of heat in the unconsolidated valley deposits, but there are a 
number of disturbing factors. Adjacent to the mountains the waters are unusually cool; 
the presence of hot springs tends to disturb conditions, and the depths from which the waters 
flow are often not known. The common rate of downward increase in temperature appears 
to be slightly less than 1° F. in 50 feet, but the facts obtained do not warrant a closer 
statement. It may be of local interest, however, to observe that in general the tempera- 
ture of the water increases with the depth of the wells at approximately that rate. 

Few measurements have been made, but it is common experience that the yield of many 
flowing wells in the area under consideration has decreased. The most comprehensive 
measurements are those made of the wells owned by Salt Lake City near Liberty Park 
(p. 44). Comparing the discharge of 12 of these wells in August, 1890, with the yield of the 
same wells in September, 1902, it appears that in the interval of twelve years the flow of 
one had increased, but that those of the others had materially decreased. Such decrease, 
however, may be due largely to clogging of the pipes, for the total yield of the Liberty Park 
area has been maintained with little decrease by sinking new wells. 

Decrease in yield is conspicuously apparent in Lehi and Spanish Fork, where flowing 
wells, formerly could be obtained much more generall3r than now, and is notable elsewhere 
throughout the valley, especially adjacent to the boundary of the flowing area. Decrease 
in flow of individual wells is soTietimes due to clogging up with sand and clay, and often 
can be remedied by cleaning or by the use of casing. But the general decrease is to be 
explained chiefly by the large increase in the number of wells which draw on the general 
supply. It is also to be remembered that for the past few years the annual precipitation 
has been considerably below the mean. 

The artesian wells are used for stock, irrigation, and domestic purposes. The amount 
used for stock is comparatively small, and, save for watering small gardens, artesian water 
as yet is not extensively used for irrigation, except locally. Probably over a thousand acres 
are thus irrigated in Utah Lake Valley, the principal areas being below Lehi and Payson. 
The artesian supply is much used for domestic purposes, and in general furnishes an admi- 
rable quality of water, containing much less dissolved salts and being much purer than 
shallow ground water. 

An attempt was made to estimate the total number of flowing wells in the area studied, 
but the result is to be taken only as a rough approximation. There are about 5,000 flow- 
ing wells in the valleys of Utah Lake and Jordan River, and possibly somewhat more than 
half of these occur in the southern valley! Assuming an average of 15 gallons a minute, a 
total yield of about 150 second-feet is thus indicated. 

Outside of the area in which flowing wells are obtained underground water is recovered 
either from shallow dug wells that tap the upper surface of underground water or from 
driven wells in which the M^ater comes from a relatively deep horizon and is under pressure 
which causes it to rise toward the surface. To save the expense of " driving," shallow wells 
are often dug within the area in which flowing wells can be obtained. Occupying the center 
of the valley and extending approximately to the limit at which flowing wells can be 
obtained, ground water lies within 10 feet of the surface, and locally, as has been mentioned, 
swampy conditions exist. As the base of the mountains is approached the depth to ground 
water increases and is over 50 feet on much of the upland where, over large areas, the dis- 
tance to water is unknown. 

Water is recovered from these wells generally by buckets and hand pumps . Comparatively 
few windmills are in operation. An average wind velocity of not less than 6 miles an hour a 
is stated to be required to drive a windmill; and since the mean wind velocity at Salt Lake 



a Wilson, H. M., Pumping for irrigation: Water-Sup. and Irr. Paper No. 1, U. S. Geol. Survey, 
?96, p. 27. 



EECOVERY OF UNDERGROUND WATER. 37 

City from June toScptomhcr, inclusive, is 6.5 miles an hour and for the entire year averages 
only 5.9 miles, the natural conditions are not very favorable for this form of power. Steam 
pumps are used only to a limited extent. The Bingham Consolidated Company has three 
.'3-inch wells 25() to 300 feet deep in which the water rises to within ai)out 70 feet of the sur- 
face; 125 gallons per minute are reported to ])e supplied hy each, the water being raised by 
compressed air. Another instance of successful pumping is at the brickyard in sec. 29, 
T. 1 3., R. 1 E., where 40 gallons a minute are reported to be obtained from a well 30 feet 
deep. Gasoline for pumping has not been much used. Electric power can be cheaply 
developed in the canyons and affords a valuable asset. In the valleys of Utah Lake and 
Jordan River pvunping on a large scale has not yet been resorted to. The^e is, however, a 
considerable quantity of water within easy reach of the surface which probably will not 
much longer remain unused. 

Underground water is recovered in exceptional circumstances by means of subsurface 
dams, or similar contrivances, which impound the underground supply. In unconsolidated 
materials, in order that this may be successfully accomplished, certain conditions are nec- 
essary. Practically impervious bottom must exist within easy reach of the surface to pre- 
vent excessive lowering of the ground-water level, and competent side walls, not too far 
apart, should be present to intercept lateral escape. The presence of the necessary condi- 
tions can be determined only by prospecting, and the practicability of such structures is an 
independent question, but because of the value of water in the area under consideration 
their feasibility should be investigated. Possible locations of subsurface dams are suggested 
by rock walls at the mouths of the narrow canyons, where borings in search of suitable bot- 
tom should be made. Tests of the amount and porosity of the valley filling at and above 
the mouths of the canyons, together with measurements of the velocity of the underflow, 
would indicate the quantity of available underground water. On Emigration Creek, for 
instance, the comparatively low run-off, suggesting an unusual amount of underdrainage, 
and the quantity of water obtained from the inefficient city trench invite further testing of 
the possibilities. Below the mouths of the canyons in the several creek valleys favorable 
conditions also may be discovered by the drill to warrant the constiiiction of infiltration 
galleries. 

In the section devoted to geology it is stated that the rocks of this region are more or less 
disturbed and broken, and an important part of the precipitation on the mountains finds its 
way into the bed rock. The water occurs in the small interstices or pores which are present 
in all rocks, in larger spaces such as fissures or solution channels, and along joints, bedding 
planes, and igneous contacts. As would be expected, less water is found in the Oquirrh 
Mountains than in the Wasatch. Bingham is a dry camp, though more or less water is 
encountere'd in the workings, while the mines of Park City are wet. The Ontario tunnel, 
which drains most of the large mines of the latter district, is stated by J. M. Boutwell to dis- 
charge from 6,(K)0 to 9,000 gallons a minute. Considerable water is being recovered by tun- 
nels driven into bed rock along the base of the mountains. In some instances the site of 
the tunnel marks the presence of a former spring, as, for instance, Wadleys, near Pleasant 
Grove, and those in Butterfield Canyon. But in one, the Dalton and Lark tunnel, east of 
Bingham, water in quantity was not encountered until several thousand feet of rock were 
penetrated. 

Another method of recovering water from b(^d rock is suggested by the structure of the 
mountains southeast of Salt Lake City. It will be recalled from the outline of the geology 
that a great syncline, modified by local undulations, is there developed, whose axis extends 
along the valley of Emigration Creek. The general structure is favorable for the occurrence 
of artesian water, but there are unfavorable complications. The rocks are chiefly compact 
limestones, the general disturbed and fissured conditions tend to relieve the pressure on the 
interstitial water, and the Wasatch fault has cut across the strata. Nevertheless, it is pos- 
sible that locally the red sandstones contain water under pressure, but because of the limited 
intake area a large supply is not to i)e expected. 



38 UNDERaROUND WATER IN VALLEYS OF UTAH. 

SUGGESTIONS. 

It is evident that in general a high degree of efficiency in the use of the water resources of 
the valleys of Utah Lake and Jordan River is not maintained. Conditions can be greatly 
benefited by preventing waste whenever possible. Most prominent in this connection is the 
conservation of storm waters. Besides the construction of large impounding reservoirs 
small ones can profitably be built at many localities within the mountains. Also to a cer- 
tain extent storm waters can be utilized by diverting them on the uplands and permitting 
them to spread over a larger area instead of allowing the run-off to escape rapidly in the 
natural channels. The effect would be an appreciable increase of the downstream seepage 
and of the replenishment of the underground store. Moreover, storm discharge may be 
lessened by planting trees and by protecting the watershed from fire, lumbering, and grazing, 
thereby promoting retention of the water by absorption and the increase of seepage run- 
off long after the storms are over. Another important loss of water occurs because of faulty 
methods of transportation for use in irrigation. As the need of economy increases more 
efficient conduits will replace crudely constructed ditches. Water thus saved, however, 
proportionally diminishes the replenishment of the underground store. Loss also occurs by 
allowing artesian wells to flow when the water is not needed. Either the wells should be 
capped or the flow at least be partly checked when water is not used, or it should be 
collected in reservoirs. 

The abundance of water in the lowlands and a dearth of it in the uplands, where the soil 
is generally fertile, free from alkali, and well adapted to the growth of fruit, suggest that a 
more efficient application of the available water supply should be practiced. Because of the 
scarcity of the underground supply on the uplands and the possibility of distributing creek 
water there by high-level canals, and since there is not enough water in the creeks to directly 
serve both the uplands and lowlands, it would appear that steps should be taken to increase 
the upland supply from the creeks and to use wells, either flowing or pumped, in developing 
the lowlands. The popularity of pumping plants in irrigation elsewhere, the proximity of 
underground water to the surface in the lowlands, and the availability of electric power 
that can be developed in the adjacent canyons are facts favorable to the proposed change. 
Moreover, seepage from the greater use of creek water on the uplands will increase the avail- 
able underground supply in the lowlands. The upland water supply may also be increased 
by the- development of springs, by tunneling into the mountains, and possibly by the con- 
struction of subsurface dams and infiltration galleries at favorable localities. 

More attention should be given to developing and preserving a pure water supply for 
domestic purposes. Surface streams should be protected from pollution, and care should be 
taken to reduce to a minimum the contamination of water in wells by using modern methods 
in the. disposal of household refuse. The common location of the towns, near the base of 
the mountains, where sufficient amounts of pure water are generally available either from 
creeks or springs renders the problem of public water supply relatively simple; yet it is a 
remarkable fact that only a few towns utilize their opportunities. 

OCCURREiy^CE OF UXDERGROLTJ^D TVATER. 

WEST OF JORDAN RIVER. 
DIVISIONS OF AREA. 

The area west of Jordan River within the region covered by this report is naturally 
divided into two parts. One is the lowland which extends from Great Salt Lake eastward 
to Jordan River and thence continues in a narrow belt southward, adjacent to the river; 
the other is the upland which, from the southern and western border of the lowland, extends 
with increasing elevation to the base of the Oquirrh Mountains. No sharp line of division 
can be drawn between these areas, for they grade into each other, yet on the whole they 
are distinct. The distribution of underground water in the two areas also is distinct, a 
convenient line of separation being that which marks the boundary between flowing and 



. S. GEOLOGICAL SURVEY 



WATER-SUPPLY PAPER NO, 167 




MAP SHOWING THE AREA IN WHICH FLOWING WELLS ARE OBTAINED IN JORDAN VALLEY. 



OOCURRENOE OF rNDERGRoUND WATER. 39 

nonflowing wells. As sliown by PI. Vll, this lino lie;j close to tlic Jordan in tlic soutlicin 
part of its course, but across the river from Murray takes a westward turn, and, following 
the base of the upland, extends to Great Salt Lake at the northern base of the Oquirrh 
Mountains. This line also roughly marks the boundary between shallow and deep ground 
water. In the lowland area ground water is abundant and generally lies within 10 feet of 
the sui-face, while on the upland water is generally scarce and is found only at a depth of 
over 50 feet. 

UPLAND AUE.\ WEST OF lOROAN RIVER. 

In general the upland has the aspect of a rollhig plain which gradually rises to the ])ase 
of the mountains, but in detail the plain is varied by the presence of benches and escarp- 
ments, relics of Lake Bonneville and of a few drainage ways that have incised channels 
across the plain. Locally, especially at the northern end of the Oquirrh Mountains and at 
the Narrows, where Jordan River flows through the Traverse Mountains, the shore lines 
of Lake Bonneville are unusually well marked. Different stages of the lake's history are 
recoi'ded by a series of distinct benches, which descend one below another from the Bonne- 
ville level; at Jordan Narrows, for instance, no less than ten periods of pause in the lake 
level are thus recorded. Shore phenomena in general, however, are less prominently 
marked on the western margin of Jordan Valley than on the eastern, adjacent to the 
Wasatch Mountains. 

Bingham Creek is the only perennially flowing stream which runs for any considerable 
extent across the plain, though Butterfield Creek flows for a short distance after it emerges 
from the mountains southwest of the town of Herriman. This area is also traversed by a 
number of arroyos which contain water only for a few days after storms and during the 
time of rapidly melting snow. The Utah and Salt Lake and the South Jordan canals, 
cariying water from the upper part of Jordan River, extend along the eastern border of 
the upland and supply irrigation water to a narrow belt. Above the upper canal the area 
is desert and practically uninhabited, except for the town of Herriman and a few scattering 
ranches which obtain local supplies of water. The Utah Lake project of the Reclamation 
Service plans to make available for irrigation a belt from 2 to 4 miles wide west of the Utah 
and Salt Lake canal, but .a large part of this upland area west of Jordan River has too great 
an elevation to be cheaply irrigated from Jordan River. Some amelioration of the present 
arid conditions may be effected by constructing reservoirs at the base of the mountains, 
but the collecting area is small and no very extensive additions to the water supply are 
likely to be derived from this source. More or less dry farming is already practiced here. 
The land is fertile, is piactically free from alkali, and because of its location would be very 
valuable if an adequate supply of water could be obtained. Unfortunately, so far as 
known, underground w^ater conditions afford little prospect of a large supply from that 
source, though valuable quantities can locally be recovered. 

This upland area is largely underlain by gravel and sand, and along the base of the moun- 
tains coarse gravel predominates. The material was derived from the disintegration of 
th(^ adjacent highlands and mostly deposited offshore in the ancient lake. The constitu- 
ents have been worked over and sorted during the did'eient stages of the lake's history, 
both by wave action and by .subaerial influences, so that the resulting material is hetero- 
geneous both as to its composition and arrangement. 

Drills have recorded only to a very limited extent the nature of the deposits that underlie 
the surface. Judging from the records and from conditions elsewhere, it is probable that 
bed rock lies not far from the surface contiguous to the base of the mountains, and that at 
a distance from the highland bed rock lies at a considerable, though unknown, depth. 
Nearer the mountains the vmconsolidated valley filling is doubtless of coarser texture 
than farther away, and it is likely that the materials are arranged lenticularly rather than 
in continuous beds. That portion of the slight precipitation on the low, small watershed 
of the Oquirrh and Traverse mountains that is not evaporated or does not join the permanent 
run-olf is absorbed by the porous deposits. Under the influence of gravity the water 



40 UNDEEGEOUND WATEE IN VALLEYS OF UTAH. 

penetrates downward until a relatively impervious layer is reached, when it tends to 
spread laterally and to slowly move toward a lower level, at the same time filling, to a 
greater or less extent, the voids in the overlying material. 

In the greater part of the area occupied by Lake Bonneville bed rock is so deeply covered 
b}^ valley deposits that it is impracticable to recover the water contained in it; but along 
the border of the old lake, where the rock outcrops, water is obtained from tunnels in a 
number of places. In the development of the Bingham mines more or less water has been 
encountered, and the town is supplied from mine tunnels. Water has also been found in 
two tunnels constructed for mining purposes near the base of the mountains. The Butter- 
field tunnel, in Butterfield Canyon, a few miles west of Herriman, encountered considerable 
water, which has caused some litigation. After the construction of the tunnel a number 
of springs tributary to Butterfield Creek ceased to flow, and suit was brought against the 
mining company by the inhabitants of Herriman. Apparently the source of the springs 
was tapped by the tunnel, and judgment was awarded against the mining company. The 
Dalton and Lark tunnel, west of the town of Lark, struck water in the spring of 1903. 
The tunnel was driven 5,000 feet through igneous rock before the water was found. It 
occurs in quartzite that is reported to be much broken and fissured. The supply was 
estimated at first to be 2,500 gallons a minute, but in the summer of 1904 this had decreased 
to about 1,500 gallons, most of which was used for irrigation at a ranch about 2 miles east 
of the mouth of the tunnel. The quantity is reported to be greatest shortly after the 
time of melting snow, thus indicating the source. The experience of these tunnels indi- 
cates in general what may be expected by driving into the Oquirrh Range. 

Springs of greater or less magnitude occur in a number of places along the base of the 
mountains. These are either supplied by seepage or by water from a deeper-seated source. 
In Rose, Butterfield, and Bingham canyons a number of springs occur, which help main- 
tain the flow of the streams. Also at irregular intervals along the border of the upland 
there are springs which, in general, supply only a few gallons a minute. A conspicuous 
locality is in the northwestern part of T. 2 N., R. 2 W., where a local area of shallow ground 
water occurs. Along the northern base -of the Oquirrh Range there is a group of large 
springs, which occur in notable alignment and apparently are associated with a fault. The 
water issues from unconsolidated debris and is slightly warm and brackish. The. springs 
have an elevation of only a few feet above the lake, however, and are too low to be of much 
service without pumping. Analysis of one, known as the Jap Pond, shows a content of 114 
grains per gallon of dissolved salts, chiefly sodium chloride. The total discharge of 9 of 
these springs in April, 1905, amounted to 8.5 second-feet, and it is reported that the flow 
remains practically constant throughout the year. 

On the upland, between the Ijase of the mountains and the canals, the little underground 
water that is recovered is obtained from wells, but in this entire region, with very few 
exceptions, ground water lies over 50 feet beneath the surface. A few wells have been 
sunk on the upland away from the lines of surface drainage, and in general they have been 
failures. The most successful wefls are along the courses of creeks and arroyos, and future 
search may be carried on with the best prospect by following these drainage ways where 
the water tends to accumulate. 

Development in Bingham Canyon illustrates the occurrence of underground water 
beneath a surface-drainage way. More or less placer mining has been carried on in the 
creek gravels, but near the mouth of the canyon, where there is a considerable amoimt 
of debris, work has been seriously interrupted by the abundance of water beneath the 
bed of the creek. It is in such places, where rock walls confine a narrow channel, that 
tests might well be made with the view of constructing subsurface dams to impound the 
underflow. 

Below the canals ground water lies nearer the surface, because of the lower elevation of 
the country and the increased supply derived by seepage from the canals. Ground water 
lies at a greater depth than 50 feet only in a narrow belt below the Utah and Salt Lake 
Canal, and in most of the area between the canals and the fine of flowing wells ground water 



OCCURRENCE OE UNDERGROUND WATP:R. 41 

can be obtained at 10 to 50 feet from the surface. The effect of irrigation on ground 
water in this area, as elsewhere, is marked. Before irrigation was practiced the depth 
to water was considerably greater than at present; for instance, it is reported that the aver- 
age level of ground water in several wells in T. 2 S., R. 1 W., now lies 30 to 65 feet nearer 
the surface than formerly. Besides this more permanent effect, the ground-water level 
fluctuates annually from 10 to 15 feet. It is also stated that the. quality of ground water 
has deteriorated in recent years, containing now much more alkali than formerly. So 
marked has this change been that surface wells are but little valued, and generally water 
for domestic use is obtained from deep wells. 

Inspection of the list of wells will show the typical facts of distribution and occurrence 
of underground water in this n'gion. It will b:' observed that many wells are about 250 
feet deep and that the range is from less than 100 feet to 1,000 feet. No careful logs 
have been kept, but from fragmentary information it appears that there is considerable 
variation in the material encountered in drilling, implying that the sediments are irreg- 
ularly sorted and that they exist in more or less lenticular arrangement. Accordingly 
there are no persistent water horizons. Water is generally found in wells wherever sand 
and gravel are encountered. In S3veral wells a number of water beds are recorded. This 
water is always under pressure; the height to which it ris;s varies, according to location 
and elevation, from close to the surface down to 100 feet below it. Generally, fairly good 
water, within easy pumping distance, is obtainable in this belt of country between the canals 
and the line of flowing wells. 

At the Cannon farm, in spc. 34, T. 2 S., R. 1 W., a well was sunk 1 ,000 feet in an attempt 
to get a flow, but although two thin water-bearing beds were found between 600 and 800 
feet, from which the water rose to within 30 feet of the surface, flowing water was not 
obtained. 

LOWLAND AREA WEST OF JORDAN RIVER. 

The lowland that lies topographically below the line of flowing wells w^est of Jordan 
River is almost a level plain which, along its margin, rises gradually toward the southwest. 
Local depressions in the plain are occupied by shallow alkaline lakes, which formerly had 
no outlet but now are drained into Jordan River. The soils of the lowland are chiefly loam 
and sandy loam, but adjacent to the lake and in local low areas considerable clay is present. « 

The nature of the underlying deposits is revealed by a number of well records, and (as 
would be expected) fine-textured materials are more abundant than nearer the mountains. 
A few deep wells have been sunk in this general region, proving the great thickness of the 
old lake deposits. The deepest is the Guff ey-Galey well, drilled near the shore of the lake, 
2 miles southwest of Farmington and about 10 miles north of Salt Lake City, in an unsuc- 
cessful search for oil.^ This well was put down 2,000 feet without encountering bed rock. 
Another deep well is that of the Rio Grande Western Railway at Salt Lake City, which 
was sunk through alternating beds of sand and clay, with very little grav(>l, to a depth of 
1,073 feet. This is the deepest well in the area undei' consideration, and its record (p. 42), 
as given by the driver, Gus Westphal, is as follows: 



a A soil survey in Salt Lake Valley: Bull. U. S. Dept. of Agriculture No 64, 19fK). 
1^ Boutwell, J. M., Oil and asphalt prospects in Salt Lake basin: Bull. U. S. (;eol. Survey No. 2(iO, 
p. 47L 



42 



UNDEKGROUND WATER IN VALLEYS OF UTAH. 



Record of Rio Grande Western Railway Company's well at Salt Lake City. 



Thickness 
in feet. 

Thin strata of clay 

and sand 130 

Clay and hardpan 40 

Red sand 30 

Clay and hardpan. . . 60 

Gray sand 5 

Clay and sand 44 

Sand 8 

Clay 20 

Sand 13 

Hard clay 6 

Sand 8 

Clay 10 

Sand 18 

Clay 20 

Sand 4 

Clay 10 

Blue sand 12 

Clay 5 

Blue sand 30 

Hard clay 10 

Sand and gravel 1 

Clay 12 

Gravel 4 

Gray sandy clay 28 

Tough blue clay 30 

Hardpan 3 



Depth in 
feet. 



1-130 
130-170 
170-200 
200-260 
260-265 
265-309 
309-317 
317-337 
337-350 
350-356 
356-364 
364-374 
374-392 
392-412 
412-416 
416-426 
426-438 
438-443 
443-473 
473-483 
483-484 
484-496 
496-500 
500-528 
528-558 
558-561 



Thickness 
in feet. 



Sand 

Soft blue clay 

Sandy blue clay 

Hardpan 

Sand 

Sandy gray clay . . . . 

Red sand 

Gravel 

Blus clay 

Clay and sand, alter- 
nating every 12 or 
18 inches 

Hardpan 

Sand and gravel 

Blue clay 

Gray clay 

Sandy gray clay . 

Quick sand 

Blue clay 

Sandy blu3 clay 

Quicksand 

Gray clay 

Fine blue sand 

Tough blue clay 

Hardpan 

Fine sand. 

Hard blue clay 



40 
40 
2 
16 
18 
36 
10 
76 

84 

8 
11 
16 
24 
13 
15 
21 
11 
10 
11 

3 
12 

2 
21 

4 



Depth in 
feet. 

561-569 

569-609 

609-649 

649-651 

651-667 

667-685 

685-721 

721-731 

731-807 



807-891 

891-899 

899-910 

910-926 

926-950 

950-963 

963-978 

978-999 

999-1,010 

1,010-1,020 

1,020-1,031 

1,031-1,034 

1,034-1,046 

1,046-1,048 

1,048-1,069 

1,069-1,073 



Although the general composition of the old lake deposits is known, not enough informa- 
tion has been accumulated to enable very definite statements to be made concerning the 
detailed distribution of the sediments. A comparison of available well records shows that 
the alternating bads of sand, clay, and gravel, generally, can not be recognized as being 
equivalent in the several wells, and from the present evidence it appears that while there 
are great thicknesses of both sand and clay, which must have a more considerable lateral 
extent than the beds nearer the mountains, the lake deposits are lenticularly arranged. 
Sinc3 no correlation has been established, the structure of the lake deposits is not known. 
Apparently they are approximately horizontal, but with a. slight inclination toward the 
lake from the highlands. This is indicated by the pressure obtained in artesian wells and 
is proved in a few instances by well records. 

In the broad lowland west of Jordan River there is an abundance of water. Throughout 
practially all of this area ground water lies within 10 feet of the surface, and water is con- 
tained in the underlying deposits down to an unknown but considerable depth. Apparently 
flowing wells can be obtained anywhere within this area. Although the water is so gen- 
erally distributed, it is profitably recovered only from the more porous, coarser textured 
deposits of sand and gravel, which constitute natural reservoirs and in which the water 
moves more readily. Accordingly, water is found at several horizons in the course of , 
sinking a deep well. In the Rudy well, for instance, 1,002 feet deep, situated in sec. 5, T. 
1 N., R. 1 W., 25 water horizons from which surface flows were obtained are reported. A 
record of this well is not available, but "good strong" flows besides minor ones were 
recorded, respectively, at 400, 508, 685, 753, and 881 feet. 

Though water is so abundant, this lowland region is thinly populated, the chief drawback 
to its settlement being the presence of much alkali in the soil over a considerable part of 



OCCURRENCE OF UNDERGROUND WATER. 43 

the area. The Bureau of Soils of the United States Department of Agriculture, in coopera- 
tion with the Utah p]xperinient Station, is at present engaged in a d(>nionstration of the 
feasibility of reclaiming this land on a farm 3 miles west of Salt Lake Cit}'. But by no 
means all of the soils in this lowland area contain excessive amounts of alkali," especially 
along Jordan River and adjacent to the border between the lowland and highland areas 
there are thriving settlements. 

The map and list of wells show general conditions. The wells are grouped along the 
margins of the area, and few are located in the interior. In general they are 2 inches in 
diameter, but they vary in depth greatly. Although flows are obtained locally at only 30 
feet bck)W the 'surface, 'commonly they are not encountered above 150 feet. Perhaps the 
avei-a^e well is between 200 and 300 feet in depth. It is a striking fact that flows may be 
obtained throughout the entire area at similar, but not at regular depths, indicating only a 
slight inclination of the water-bearing horizons and their lenticular character. The flows 
are usually small, averaging perhaps under 5 gallons a minute, though there are a number 
of 15-gallon flows. The supply generally is reported rather constant, except that the 
shallower well& a?e sirbject to seasonal variation. The pressure obtained, too, generally 
is small, being only enough to cause the water to rise either barely to the surface or a few 
feet above. In general the pressure and the flow are reported to increas.^ with the depth 
but measurements are not available. Both the flow and the pressure are considerable 
in the deep Rudy well, sec. 5, T. 1 N., R. 1 W. 

The conditions here noted apply mostly to the areas contiguous to the eastern and 
southern borders of the lowland west of Jordan River. Little information is available 
concerning the rest of this area (see list of wells pp. 59-75.) The few wells near Great Salt 
Lake were sunk to unusual depths beforeflowing water was obtained, this being apparentl}' 
due to the greater development of clay in that region, though no complete logs have been kept. 
The well at the Inland Crystal Salt Company's works, in which, at a depth of 560 feet, water 
was struck which rises about 9 feet above the surface and flows about 10 gallons a minute, 
is reported 720 feet deep. Underground water in the Pleistocene deposits near the lake 
contains considerable salt. 

EAST OF JORDAN RIVER. 

East of Jordan River the occurrence of underground water will be described under 
the following heads: Salt Lake City, lowland area south of Salt Lake City, and upland 
area south of Salt Lake City. 

SALT LAKE CITY. 

Salt Lake City is built principally on the floor of the main valley, ))ut its outskirts 
extend northward on the old delta of City Creek and eastward on the benches at the base 
of the Wasatch Mountains. Adjacent to the highlands the underlying deposits are very 
irregular in composition and distribution, consisting of sand and gravel with intercalated 
streaks of clay. But toward the valley proper the conditions become more regular and 
the prevailing clay is interbedded with sand and gravel, though from the records obtained 
no definite sequence appears to be applicable to any considerable area. 

In the lower purt of the city marshy areas occur, but conditions there have been much 
improved since the early days of settlement. Formerly the lower chaimels of City, Red 
Butte, Emigration, and Parleys creeks were ill defined and at high-water stage the part 
of the city adjacent to Jordan River was a great slough. But by erecting embankments, 
by confining the creeks to definite channels, and by draining the western part of the city 
much of the swampy land has been reclaimed. Shallow ground water, except on the 
benches, generally lies within 10 feet of the surface. 

The line separating flowing and nonflowing wells skirts the lower benclu's, so that in 
the larger part of the area occupied by the city artesian wells are obtained: Flows are found 

oSoil survey in Salt Lake Valley: Bull. U. S. Dept. Agric. No. 64, 1900. Reclamation of Alkali 
anda: Fifth Rept. Bureau of Soils, 1903, p. 1144. 



44 



UNDERaROUND WATER IN VALLEYS OF UTAH. 



at different horizons from about 50 feet downward, a common depth of wells being between 
100 and 300 feet. The deepest well is that of the Rio Grande Western Railway Company 
near its station, the record of which appears on page 42. This well is 4 inches in diameter 
and 1,073 feet- deep. It was put down in 1895 and 15 horizons were passed through from 
which flows were obtained. At a depth of 1,048 feet the greatest flow occurred, amounting 
to 78 gallons a minute at 4 feet above the surface and to 37.5 gallons at ,25 feet above. 
The most notable group of wells in this vicinity is that put down by Salt Lake City adjoining 
Liberty Park. There are 16 or more of these ranging from 2 to 9 inches in diameter and 
from 100 to 600 feet in depth. About half a dozen different water-bearing horizons, each 
furnishing a flow, are said to have been encountered in driving the wells. The greatest 
pressure reported caused the water to rise in a pipe 35 feet above the surface. Discharge 
measurements, as furnished by the city engineer, are given in the following table: 

Discharge of city wells near Liberty Parle, Salt Lake City. 



No. of 
well. 

1.... 
2.... 
3.... 

4.... 
5.... 
6.... 
7.... 
8.... 
9..-. 


Diam- 
eter. 

Inches. 
9 
9 
8 
8 
8 
2 
2 
2 
2 


Date of measurement. 


No. of 
well. 


Diam- 
eter. 


Date of measurement. 


Aug. 10, 
1890. 

- 


July 17, 
1900. 


Sept. 29, 
1902. 


Aug. 10, 
1890. 


July 17, 
1900. 


Sept. 29, 
1902. 


Gallons. 
201,600 
180,000 
279, 132 


Gallons. 
120,000 
297,000 
280,000 
215,000 
5. 000 


Gallons. 

96,941 

60, 588 

302,940 

193,882 

11,459 

5,876 

610 

206 

19,784 


10.... 
11.... 
12.... 
13.... 
14.... 
15.... 
16.... 


Inches. 
2 
2 
2 
2 
2 
9_ 
2 


Gallons. 
43,200 
33,230 
36, 000 
54,000 


Gallons. 
38,000 
19,000 
16,000 
35,000 
18,000 
98,000 
6,000 


Gallons. 
35, 644 
15,892 
14,213 
20,626 
13,316 
36, 172 
2,844 


59, 040 


14,400 10.000 




16,000 
27,000 
54,000 


1,000 

500 

25,000 






997,602 


1,183,500 


830,993 



In the immediate vicinity of these wells there are a number of springs whose supply is 
maintained chiefly by seepage. The combined flow from these springs and wells is esti- 
mated to amount to a maximum of 2,500,000 gallons a day. In order to utilize this 
supply in the city mains a pumping plant would have to be installed, and a further dis- 
advantage is the doubtful quality of the water. At present this source is used for street 
sprinkling and for feeding the lake in Liberty Park (PI. I). 

In the northern part of Salt Lake City several thermal springs occur, the most conspic- 
uous of which are the hot and warm springs. The hot springs issue at a temperature of 
about 130° from the Wasatch limestone at the western end of the spur of the mountains, 
with a discharge of about three-fourths second-foot,a and flow into Hot Springs Lake. 
The warm springs issue from unconsolidated deposits at the base of the spur about 2 miles 
southeast of the hot springs. The water is pumped to a slight elevation, from which it is 
piped to a sanitarium, the amount delivered being reported to average 350 gallons a minute. 
The temperature is 118° at the springs and about 100° at the sanitarium. Several other 
similar, but less important, springs occur, associated with the great Wasatch fault, along 
the base of the mountains between hot and warm springs. 

The municipal water supply of Salt Lake City is derived from mountain streams and dis- 
tributed through city mains. From this source there is an excellent supply of pure water 
under good pressure. The chief near-by available streams are City, Red Butte, Emigra- 
tion, Parleys, Mill, Big Cottonwood, and Little Cottonwood creeks. The discharges of 
some of these are given on pages 19-22. None of these except City Creek is entirely con- 
trolled by the city. Red Butte Creek is reserved for the army post at Fort Douglas, Emigra- 
tion and Parleys creeks partly contribute to the city supply, and the others are used entirely for 



a Measured by A. F. Doremus. 



OCCURRENCE OF UNDERGROUND WATER. 45 

irrigation and domestic purposes, under water rights owned hy farmers. In order for 
Salt Lake City to utilize these streams it must huy the water rights or exchange with the 
farmers an equivalent amount of water obtained either from Utah Lake or from pumping 
plants. 

The present public supply accordingly is obtained from City, Parleys, and Emigra- 
tion creeks. The watei-slied of City Creek is protected from forest fires and from contam- 
ination, and many of its springs are developed. The flow is distributed from settling tanks 
near the mouth of the canyon and from a reservoir on Capitol Hill having a capacity of 
approximately 1,000,(J00 gallons. The surplus waters of City Creek are allowed to escape 
through flood ditches. Water from Parleys Creek to the extent of 81.8 per cent of its flow 
has been obtained by Salt Lake City in exchange for an equivalent amount of water from 
Utah Lake delivered through the Jordan and Salt Lake City canal. A settling reservoir, 
holding somewhat less than 1,000,000 gallons has been constructed at the mouth of Parleys 
Canyon, whence the water is conducted through a concrete conduit to a storage reservoir 
with A capacity of about 5,000,000 gallons situated on Thirteenth East street. An addi- 
tional supply is obtained from a trench in the bed of Emigration Creek half a mile above 
the mouth of the canyon. This trench is approximately 150 feet long, 10 feet wide, and 
18 feet deep. It was dug in sand and gravel in the bed of the creek and at right angles to 
its course. A supply estimated to amount to 1,000,000 gallons a day is thus obtained, which 
is piped to the Thirteenth East street reservoir. 

No direct record is kept of the amount of water used by Salt Lake City, but discharge 
measurements of the creeks at the mouths of the canyons show the amount available. 
This is insufficient during the dry months and the use of water is restricted to a per capita 
consumption of 120 gallons a day, although it is considered desirable, in this dry climate, 
where lawns and gardens have to be irrigated, to maintain a per capita supply of approx- 
imately 300 gallons a day. It is planned to obtain in the immediate future a portion of the 
flow of Big Cottonwood Creek, by exchanging therefor water from Jordan River, delivered 
through the City canal, as is being done in the case of Parleys Creek, and to make the new 
supply available by constructing a pipe line from the mouth of Big Cottonwood Canyon to 
the mouth of Parleys Canyon, a distance of about 7 miles. 

SOUTH OF SALT LAKE CITY. 

Lowland area. — It will be convenient to divide the area south of Salt Lake City into a 
lowland and an upland portion, taking as the dividing line that which separates flowing 
and nonflowing wells. PI. VIII shows that this line extends contiguous to, but below, 
the Jordan and Salt Lake City canal as far as Little Cottonwood Creek, after crossing 
which it turns westward to the flood plain of Jordan River. The lowland area is traversed 
by Parleys, Mill, Big Cottonwood, and Little Cottonwood creeks, which flow in open valleys, 
with broad and low intervening divides. The general aspect of the country is that of a 
slightly dissected plain that rises gently toward the upland terraces. This area is relatively 
thickly populated, and intensive farming is widely practiced. 

The detailed character of the underlying lake sediments is not satisfactorily known, but 
from the well records conditions appear to be similar to those found elsewhere in the 
area under consideration. Beneath the lowlands the stratigraphy is more uniform than 
nearer the base of the mountains; fine-textured sediments are more abundant than coarse, 
and clay predominates. But a comparison of available well records fails to establish a 
correlation between the difl'erent beds of sand and gravel throughout the lowland. Well 
drivers state that all logs are different, and yet that, on the whole, general sections persist 
for certain areas in which the difl'erences are minor. It is believed that the sediments 
slope toward Jordan River at about the same angle as does the surface. The best-defined 
sequence that has been reported occurs immediately south of Salt Lake City, where in 
general light-colored clay at the surface overlies blue clay ranging from 30 to 70 feet in 
thickness, beneath which water-bearing sands and gravels occur at a depth of about 100 



46 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



feet. At greater depths the succession appears to be more variable, but there are few 
satisfactory well records. 

Ground water now lies within 10 feet of the surface over practically the entire lowland 
area, but it is reported that in the early days it did not lie so near over so large an area. 
Present conditions are largely due to irrigation. Several old residents state that below 
the level of the Jordan River canals the ground-water surface has locally risen 40 or 50 
feet since their construction. It has already been mentioned that along several of the 
drainage ways seepage water reappears at the surface and occasionally forms considerable 
streams, as at Spring Creek near its junction with Big Cottonwood Creek, where the Septem- 
ber flow is estimated to amount to 14,000,000 gallons a day. In many places also, especially 
along the bases of benches, lines of seep springs occur that furnish considerable flows, a 
notable occurrence being those at the nursery in the southeastern part of Salt Lake City. 
But locally, as along the bluff east of Jordan River, north of the Bingham Junction 
smelters, the water appears at so low an elevation as to be of comparatively little use. 
When pumping becomes more generally practiced in the valley this ground water that lies 
so near the surface can be easily developed. 

Flowing wells in this area are numerous. They are generally 2 inches in diameter and 
100 to 400 feet in depth, and they commonly yield between 20 and 50 gallons a minute, 
though there are many variations. The pressure is low, generally less than '10 pounds. 
Well drivers say that their best results are obtained in belts extending northwest and 
southeast, parallel with the creeks, and that these productive belts are separated by rela- 
tively barren ones. The water-bearing sands and gravels apparently mark the courses 
of old waterways, while finer-textured material was deposited in the intervening areas. 
These distinctions have been noticed only in the upper parts of the lowland area, and near 
the river they are said to disappear. One of the best wells is at the plant of the American 
Smelting and Refining Company at Murray. It is 4 inches in diameter, 400 feet deep, and 
is reported to flow about 400 gallons a minute under a pressure of 3 pounds per square inch. 
The record of this well is given as follows, on the authority of H. F. Yeager, well driller: 



Record of American Smelting and Rejining Company's well at Murraij. 



Thickness 

in feet. 

Sand and gravel 5 

Mud 3 

Sand and gravel 4 

Blue clay 6 

Quicksand 10 

Blue clay 8 

Loose sand and gravel (good 

pump well at 42 feet) 16 

j31ue clay 8 

Quicksand (flow at 63 feet) 6 

Blue clay 18 

Yellow clay. 6 

Loose sand and gravel (strong 

flow at 95 feet) 15 

Yellow clay 3 

Coarse gravel and rock (strong 
flow at 112 feet, and at this 
point the well at office 

stopped flowing). 8 

Coarse gravel and rock 6 

Quicksand 20 

Clay, very hard 10 

Quicksand 6 

Gravel (small flow at 165 feet) 11 



Depth 

in feet. 

0-5 

5-8 

8-12 

12-18 

18-28 

28-36 

36-52 
52-60 
60-66 
66-84 
84-90 

90-105 
105-108 



108-116 
116-122 
122-142 
142-152 
152-158 
158-169 



Thickness 
in feet. 

Hard pan, very hard 8 

Blue clay 6 

Quicksand (flow at 203 feet) . . 20 

Quicksand 16 

Blue clay 4 

Quicksand 7 

Blue clay . 8 

Quicksand 18 

Blue clay and quicksand in 

layers 2 feet thick 22 

Quicksand . 8 

Blue clay, very hard 12 

River sand 2 

River sand 7 

Cemented gravel 12 

Yellow clay . 7 

Cemented gravel 17 

Loose gravel 23 

Yellow clay 2 

Gravel. 7 

Cemented gravel 12 

Loose gravel 12 



Depth 
in feet. 
169-177 
177-183 
183-203 
203-219 
219-223 
223-230 
230-238 
238-256 

256-278 
278-286 
286-298 
298-300 
300-307 
307-319 
319-326 
326-343 
343-366 
366-368 
368-375 
375-387. 
387-399 



OCCURRENCE OF UNDERGROUND WATER. 47 

Decrease in flow and complete failure of some wells are reported throughout this area 
and are especially apparent in the vicinity of Murray. These results are directly traceable 
to the increased number of wells that have been sunk in recent years and to the fact that 
little economy is exercised in the use of the water. Well owners should more fully realize 
that the limited water supply comes from a common source, that the wastefulness of one 
counteracts the prudence of another, and that the common interest of all demands that 
the supply be conserved. 

Upland area. — The upland south of Salt Lake City includes the area lying between the 
base of the Wasatch and Traverse mountains and the area in which flowing wells can be 
obtained. This region is characterized topographically by the abundance and perfection 
of development of shore phenomena which mark different stages in the history of Lake 
Bonneville. As on the western side of the valley, the upland is in general a plain that 
rises toward the base of the mountains, but is interrupted by benches and escarpments 
and deeply cut by the creeks flowing from the Wasatch Mountains. 

The Bonneville terrace extends along the mountains like a narrow shelf, its horizontal 
lines contrasting strongly wdth the deep, vertical furrows on the mountains. Broad deltas 
formed by the larger creeks at the Provo stage extend down to the lowlands, and successive 
escarpments mark halting places in the retreat of Lake Bonneville. The most prominent 
of all the shore phenomena in the area covered by this report is the great embankment at 
the point of the mountains east of Jordan Narrows. Here the waves, gaining energy from the 
wide expanse of the old lake, carved a great sea cliff against the mountains and distributed 
the debris to form an enormous accumulation of sand and gravel. 

Prominent local features of this upland belt are the relics of glaciers adjacent to the mouth 
of Little Cottonwood Canyon and the evidences of recent faulting along the base of the 
mountains. Little Cottonwood Creek in Pleistocene time was occupied by a glacier which 
carved a broad U-shaped valley and deposited lateral and terminal moraines composed of 
a heterogeneous mass of coarse- and fine-textured debris. Along the entire front of the 
Wasatch Mountains Gilbert has found indications of recent dislocation associated with the 
great Wasatch fault. The evidence is varied, but escarpments in unconsolidated material 
breaking the even trend of alluvial slopes are conspicuous. 

The underlying deposits of the upland are mostly coarse textured, being near their origin, 
and consist chiefly of sand and gravel. The creeks, where they have cut deeply, expose 
good sections, but few deep-well records were obtained. 

This region in general is thinly populated, but where water is available there are settlements, 
and wherever the canals extend there are thriving farms. The contrast between the 
flourishing area which is supplied with water and the dry, barren region is striking. The 
map shows the distribution of the principal canal systems, which are supplied by the several 
creeks that flow from the Wasatch Mountains and by Jordan River. Underground water 
is used only to a limited extent. PL VI and the list of wells illustrate conditions. Under- 
ground water is recovered chiefly in the lower (western) part of the upland, where it lies at 
depths ranging from the surface to 50 feet below. In this productive area both dug and 
driven wells are used. The driven wells are commonly 50 to 200 feet in depth, and water 
is generally found beneath a bed of clay in sand or gravel under sufficient pressure to cause 
it to rise within pumping distance of the surface. 

In the eastern part of the upland area ground water generally lies at a greater depth than 
50 feet below the surface, and in a number of places has not been found in test wells over 
100 feet deep. In this (eastern) division of the upland, where the greater part of the valley 
deposits are coarse textured, the ground water sinks deep before a relatively impervious 
bed is encountered, and then it tends to move to the lower part of the valley. Away from 
the influence of seepage from the creeks little water is supplied to this area. Between the 
creeks the chief source of supply is seepage from the mountains. The most likely localities 
for sinking wells are along the courses of waterways, but over a large part of the upland the 
prospect is poor for obtaining imderground water in quantity within easy reach of the sur- 
face. In the mouths of the canyons there is the chance of developing the underflow by 



48 UNDEKGROUND WATER IN VALLEYS OF UTAH, 

subsurface dams or by tunnels, mentioned on page 40. Other favorable localities for pros- 
pecting are adjacent to the base of the mountains, where water may be had by developing 
springs and by tunneling into the bed rock. 

Seep springs occur at several localities along the base of the mountains south of Salt Lake 
City, the most important, perhaps, being those about midway between Mill and Big Cotton- 
wood canyons. The feeble springs there issuing from sand and gravel were formerly allowed 
to go to waste, but by developing them a flow of about 2 second-feet was obtained, and a 
considerable tract of land thus became available for agriculture. About 4 miles southwest 
of the town of Draper, in sec. 12, T. 4 S., R. 1 \7., at some distance from the base of the 
mountains, there are four warm-water lakes that are fed by springs, some of which are said 
to be quite hot. The westernmost of the group is the largest and covers an area of about 5 
acres. The temperature is reported to remain at about 70° the year round. 

Since underground water is so scarce beneath the upland, the most efficient manner of 
developing this area appears to be by the use, as suggested above (p. 38), of creek water in 
high-level canals to a greater extent than is now practiced. 

UTAH LAKE VALLEY. 

The following description of the occurrence. of underground water in the valley of Utah 
Lake begins at the north and proceeds east, south, and west around the lake, the several 
towns affording subheadings for convenient reference. (PI. VIII.) 

LEHI AND VICINITY. 

Lehi is situated in the main valley at some distance from the distinct terraces. Dry 
Creek lies adjacent to the town, but, as its name signifies, the creek, after supplying a num- 
ber of irrigation ditches, usually carries little or no water in its lower course. There is no 
public water system in the town, and the supply for domestic purposes is derived from 
numerous wells. A few shallow dug wells tap ground water at depths of 5 to 30 feet, but 
the majority are deeper and reach water under pressure. The sugar-plant mill pond is fed 
by springs and is an important local source of supply. 

Lehi was one of the first towns where artesian water was found in the Bonneville area, 
flowing wells having been obtained there about 1880. Formerly a feeble first flow was 
found in gravel about 60 feet from the surface and a stronger supply at a depth of about 
160 feet, but in recent years flows, even from the second horizon, have failed during part 
of the season in consequence of the increased use of artesian wells in the area nearer the 
lake, and at times pumping has to be resorted to. However, when water does not 
actually flow it rises in the wells to within a few feet of the surface. 

The general section in the vicinity of Lehi, as reported by H. C. Comer, shows blue clay 
to a depth of 50 or 60 feet. Below this is the first water bed, consisting of about 50 feet 
of sand and gravel, separated from the second water horizon by 40 feet of light clay. This 
section does not apply in the eastern part of the town, where the log of the San Pedro Rail- 
road well shows coarse-textured material within 100 feet of the surface. In this well the 
main supply is derived from a depth of 330 feet, the water rising to within a few feet of the 
surface. These two logs illustrate the variability of adjacent sections. 

The Utah Sugar Company's plant at Lehi has several 2-inch wells, and the following flows 
in gallons per minute are reported: 80 feet, 15 gallons; 120 feet, 25 gallons; 150 feet, 20 
gallons. Logs of these wells were not kept. The Rio Grande Western Railway well near 
the sugar factory is 3 inches in diameter and 165 feet deep. The water is reported to rise 
in a pipe to a point 30 feet above the surface and to flow about 50 gallons a minute at the 
level of the ground. 

Toward Utah Lake, below Lehi, there is a considerable development of flowing wells 
from which a number of square miles are irrigated. In this district there are several 
hundred flowing wells which average about 150 feet in depth. A close relationship has 
been established between the flow of the wells in the fields below Lehi and those in town. 







MAP SHOWING THE AREA IN WHICH FLOWING WELLS ARE OBTAINED IN UTAH LAKE VALLEY. 



OCCURRENCE OF UNDERGROUND WATER. 49 

During the irrigation season, when the field wells are all flowing, those in Lehi practirally 
stop, hut during the winter it is a general custom to plug the wells used for irrigation, after 
which those in town begin to flow. Measurements liavc not been made, but the general 
facts are well established. 

Northwest of Lehi the line separating the areas of flowing and nonflowing wells continues 
to Jordan River, reaching it 3 to 4 miles north of Utah Lake. The line extends about half 
a mile west of the river and approaches close to the northv/est corner of the lake near Sara- 
toga Springs. In the flood plain of Jordan River flows can probably be obtained continuing 
into Salt Lake Valley, but outside of the line indicated the surface elevation is too great. 

The Salt Lake City authorities, about 1890, sank a number of wells in the flood plain of 
Jordan River in sec. 12, T. 5 S., R. 1 W., with the object of increasing the supply of the 
Jordan and Salt Lake Canal. These wells, about 130 in number, were mostly 2 inches in 
diameter, though a few were 6 inches, and arc said to average 100 feet deep. Clay was 
encountered down to the bottom of the wells, which were in gravel. It is stated that 
water rose in pipes 30 to 40 feet above the surface, and that individual wells flowed 125 
gallons a minute. It is also stated that the combined flow amounted to 3,000,000 gallons 
a day. These wells soon interfered with neighboring ones, stopping their flow, and suit 
was brought against the city, with the result that the municipality was compelled to plug 
up its wells. After these had been plugged for some time a number of them were tempo- 
rarily opened, and in about twenty-four hours thereafter the water in one of the wells, the 
flow of which was interfered with, situated about half a mile above the city wells, had fallen 
25 feet. The city wells were then capped again and in five hours the water in the well 
referred to had regained 7 inches of its lost level. 

Near the northwestern end of Utah Lake there is a group of hot springs which occin* both 
on shore and in the lake. On the shore there are several springs which support the Saratoga 
resort where the water, having a temperature of 111°, issues through the lake deposits and 
is used for ])athing and to a limited extent for irrigation. In the summer of 1904, during 
the survey of Utah Lake by G. L. Swendsen of the Reclamation Service, three groups of 
springs were found beneath the water of the lake. Their existence was shown by the pres- 
ence of depressions occupying areas of 100 square feet to 3 acres in extent and having depths 
of 20 to 80 feet. Since the prevailing depth of the lake is much less and the bottom is com- 
posed of slimy mud, a considerable discharge is thus indicated. Hot water that flowed 
above the lake surface was obtained by sinking pipes a short distance into the bottom. 

About 5 miles up Dry Creek from Lehi is the town of Alpine, located near the mouth of 
the canyon on the dissected Bonneville terrace. The settlement is supplied with water 
from irrigation ditches, and possibly not more than half a dozen wells have been sunk. 
These are 25 to 80 feet deep, and the water level is reported to vary considerably between 
winter and summer. Springs occur in Dry Creek Canyon, but they have not been developed. 

AMERICAN FORK, PLEASANT GROVE, AND VICINITY. 

The towns of American Fork and Pleasant Grove receive their main water supplies, 
respectively, from American Fork and from Battle and Grove creeks. These streams 
feed a number of irrigation canals, and are the chief source of underground water in this 
vicinity. (PI. IX, B.) 

American Fork is built at the base of a series of terraces on both sides of American 
Fork (creek), which has cut a narrow chaiuiel through the old lake deposits. Ascending 
the valley from American Fork, five distinct terraces can be traced up lo the broad Provo 
bench, between which and the Bonneville level, which forms a shelving bench against the 
mountains, traces of shore lines of pre-Bonneville age have been reported. In its lower 
course American Fork is dry throughout most of the year in consequence of th(> draft 
upon its waters for the canal system which supplies the uplands. 

Shallow wells in American Fork are commonly less than 50 feet in depth, avcMuging 
possibly 25 to 30 feet, and the ground-water level is reported to vary 10 to 15 feet between 
the winter minimum and summer maximum. The water generally is found in gravel. 
IRR 157—06 4 



50 (JKDERGTIOUND WATER IN VALLEYS OF UTAH. 

Deep wells have been sunk in the extreme southwestern part of the town in search of 
flowing water. The water rises in these nearly to the surface, and furnishes the main sup- 
ply for domestic purposes. Well records show a variable succession of sand and gravel, 
with comparatively little clay. The city well is typical, and probably is the deepest in 
this vicinity. It is 440 feet deep and 6 inches in diameter. Two principal water hori- 
zons are reported, at 240 and 340 feet, and the water stands in the well at a depth of 22 
feet. An electric motor pump supplies water for public purposes, but there is no water- 
works system. Individual families or groups of famihes maintain their own wells. 

The line separating the areas of flowing and nonflowing wells as mapped between Lehi 
and Pleasant Grove lies contiguous to the San Pedro Railroad, and here, as elsewhere, 
ground water commonly lies within 10 feet of the surface. Extensive areas of marshy 
land lie contiguous to the lake shore, where conditions have grown worse since the intro- 
duction of irrigation. The flowing wells in this vicinity vary in depth, but are commonly 
about 100 feet deep. As Utah Lake is approached more nearly uniform conditions are 
revealed by the logs. Clay is commonly present at the surface and continues to a depth 
of 90 or 100 feet, below which the water-bearing gravel occurs. In the deeper wells alter- 
nating sand, clay, and gravel are reported below the first gravel, and flows are obtained 
from every coarse-textured bed. One of the best wells in this vicinity is in sec. 23, T. 5 
S., R. 1 E. It is 147 feet deep, 2 inches in diameter, and throws a stream 3 feet 8 inches 
above the pipe, having a capacity, therefore, of about 150 gallons a minute. 

A disturbed belt of rocks, dipping eastward, and locally covered by debris, lies near 
the foot of the Bonneville terrace between American Fork and Grove creeks. Springs 
occur at about this horizon, and prospecting for water in this belt, in sec. 17, T. 5 S., R. 
2 E., has brought notable results. William Wadley & Sons, by tunneling into bed rock, 
have developed enough water to irrigate a number of acres of fruit land, which is bringing 
in handsome returns. Several tunnels have been dug, the most important of which lies 
about 200 feet below the Bonneville level and was driven 318 feet through black shale 
into broken and cavernous gray limestone, in which the water occurs. 

Pleasant Grove is located on alluvial slopes formed by Battle and Grove creeks. Its 
situation is so high that flowing wells can be obtained only in the extreme lower part of 
the town, which depends for its chief underground supply on wells from which water has 
to be pumped. Ground water can usually be obtained at 10 to 50 feet from the surface. 
No regular sequence of deposits underlies the town, but a variable succession of clay, sand, 
and gravel is encountered in wells, the water horizon usually being underlain by clay. In 
the southeastern part of Pleasant Grove no successful wells have yet been obtained, though 
prospecting for them has extended to a depth of 100 feet; not deep enough to find an 
impervious stratum. A continuous succession of gravel beds is reported. 

The high, almost flat Provo delta between Pleasant Grove and Provo is scantily pro- 
vided with water. The surface is generally gravel covered, and gravel is commonly found 
in wells to depths of 30 to 60 feet, below which sand is reported. Only a small amount of 
clay appears to be present. This tract of land is well adapted for the cultivation of fruit, 
but the present supply of water is insufficient for its complete development. Water was 
first brought to the delta by canals from Provo River in 1868, and the present supply, 
whereby a maximum diversion of about 116 second-feet is obtained, was established in 1888. 
Before irrigation was practiced on the bench the depth to ground water was considerably 
greater than it is now. Old wells are over 100 feet deep, but of late years the ground- 
water surface has risen so that on a large part of the area water can be obtained in wells 
averaging 50 to 75 feet deep. Toward the lower margins of the bench the depths to ground 
water is less than 50 feet. Here, as elsewhere throughout this entire area, ground water 
is lowest in the winter and highest during the irrigation season. The annual variation 
on Provo bench appears to range from 5 to about 17 feet. A few examples will illustrate 
general conditions. In 1875 a dry well 100 feet deep was dug in sec. 14, T. 6 S., R. 2 E. 
In the same section, during the winter of 1878-79, N. Knight dug a well 110 feet deep which 
afforded 3 feet of water in winter and 15 to 20 feet in summer. In 1899 N. J. Knight 



U. S. GEOLOGICAL SURVE> 



WATER-SUPPLY PAPER NO. 157 PL. IX 




A. VALLEY OF PROVO RIVER BELOW MOUTH OF CANYON, LOOKING NORTH. 
Shows Provo Bench and Bonneville terrace. 




B. AMERICAN FORK AT MOUTH OF CANYON. 



OCCURRENCE OF UNDERGROUND WATER. 51 

dug a third well only 60 feet deep, near the second, which afrordcd about 3 feet of water 
in ^\inte^ and 20 in summer.^ 

Flowing wells can not be obtained on the bench because of its elevation, though several 
attempts have been made, without success. In 1887 and 1888 two deep wells were driven 
in the same section as those just referred to. The Colorado Fish Company put down a 
3-inch well 250 feet deep and obtained water which rose to within 80 feet of the surface. 
This was pumped for several years. In 1888 Mr. Knight drove a 2-inch well 300 f(>ct 
deep in which water rose to within 90 feet of the surface. Both of these wells are now 
abandoned. 

From Provo to Pleasant Grove along the narrow belt of lowland lying between Provo 
bench and Utah Lake there is an abundance of underground water. The line that sepa- 
rates flowing and nonflowing wells coincides approximately with the San Pedro Railway, 
which also marks roughly the upper limit of the area in which ground water lies within 
10 feet of the surface. Between the railroad and the base of the bench few wells have 
been driven and little is known of the conditions, but it is thought that water can be 
obtained at depths of 10 to 50 feet. 

Contiguous to the railroad a number of feeble seep springs occur along the base of a 
low bluff between which and the lake the ground is almost flat. Water occurs on the 
surface in many places, rendering the land unfit for use. Before irrigation was so exten- 
sively practiced it is reported that this lowland belt was fertile farming land, but in late 
years, due to the rise of the ground-water level, the land has materially decreased in value. 
Considerable areas of available land, however, are yet to be found in this area, and flowing 
wells are used to irrigate several hundred acres. Conditions can be much improved by 
drainage. The map and list of wells show the general conditions. The deep wells in 
this belt average slightly ov^r 100 feet and generally are 2 inches in diameter. North 
of Provo River the yield is inconsiderable, averaging, possibly, less than 15 gallons a minute 
pel*- well; but in the vicinity of Geneva, a resort on the lake below Pleasant Grove, the 
effect of Battle Creek drainage is experienced, and some of the strongest wells of the entire 
area covered by this report occur. Harry Gammon's wells, in sec. 7, T. 6 S., R. 2 E., are 
among the best. One of these is 3 inches in diameter, 110 feet deep, and jHlelds a flow of 
about 266 gallons a minute, the water rising in a pipe to approximately 28 feet above the 
surface. The section in this vicinity is shown on PI. V, the water occurring in gravel in 
the bottom of the well. 

PROVO AND VICINITY. 

Provo derives its water supply from Provo River. A number of canals tap the river 
(as shown on the map, PI. VIII), and distribute a good supply to the town; and water 
for household purposes is delivered through city mains from a direct source in the river 
near the mouth of the canyon. The quality is unsatisfactory, however, and a new system 
is being installed whereby a better supply is obtained from a number of springs that issue 
from unconsolidated debris along the base of the canyon for several miles above its mouth. 

Well records show fairly uniform stratigraphic conditions about Provo. Gravel usually 
imderlies the surface to a depth of from 10 to 20 feet, and is succeeded by 20 to 30 feet of 
sand, below which is a considerable thickness of clay, averaging possibly KK) feet, the 
upper 20 or 30 feet of which is yellowish and the lower part blue. Underlying the clay a 
bed of gravel occurs, which is said to be underlain by clay, though about Provo it has sel- 
dom been penetrated. With minor variations this section appears to hold good over a 
large part of the territory adjacent to the east shore of Utah Lake. Northwest from Provo 
the surface gravel disappears, but clay, light above and dark below and underiain by sand 
and gravel, is reported in the vicinity of Geneva, American Fork, and Lehi. South of 
Provo, in the vicinity of Springville, similar conditions prevail. (PI. V.) 



"These facts were obtained from Mr. Caleb Tanner, to whom the writer is indebted for many 
courtesies. 



52 UNDERGROUND WATER IN VALLEYS OF UTAH. 

The beds about Provo appear to dip toward the lake at a low angle, approximately cor- 
responding to the slope of the surface, this being indicated by the fact that the depth at 
which the water-bearing gravel, is found over large areas is approximately constant. In 
the vicinity of Provo some direct data were obtained on this point. Wells have been driven 
along Center street from Academy street in Provo westward to the shore of the lake. The 
depths at which the top of the gravel was struck in some of these wells was obtained from 
the driver, J. Westfall, and a line of levels was run along the surface by the United States 
Reclamation Service, from which it appears that the lakeward inclination of the gravel is 
approximateljT^ 9 feet per mile, the rate decreasing as the lake is approached. Similar 
conditions probably exist throughout the area studied, the slope being greatest near the 
mountains, while beneath the broad lowlands the strata lie more nearly horizontal. 

Ground water in the vicinity of Provo can generally be obtained in the upper gravel 
within 10 feet of the surface. In the vicinity of the lake the gravel disappears and clay 
generally occupies the surface. Here, as is so general throughout the entire area, swampy 
conditions prevail, owing to the lowness of the region, the recession of the lake, and the 
rise of ground water due to irrigation. 

Flowing wells exist in great numbej- in this well-populated region, and in general an 
abundance of good water is obtained within 200 feet of the surface. The main water-bear- 
ing horizon is the bed of gravel that underlies the blue clay. Water is generally reached 
in this gravel at ] 50 to 200 feet from the surface, but conditions are not absolutely uniform 
at all places, and where the prevailing section is varied by local streaks of clay, sand, and 
gravel corresponding differences exist. Feeble flows are sometimes found at 100 feet, and 
a few wells obtain water from a depth of 360 feet, but this depth is unusual in the vicinity 
of Provo. The wells about Provo are generally 2 inches in diameter, and their flow may 
possibly average 50 gallons a minute. Among the best wells in this vicinity are those at 
the stations of the San Pedro, Los Angeles and Salt Lake Railroad and the Rio Grande 
Western Railway. These are 3 inches in diameter and 190 and 176 feet deep, respectively. 
In November, 1904, the Rio Grande Western well was found to flow approximately 120 
gallons a minute at 2 feet above the surface under a pressure of 15^ pounds per square inch. 

SPRING VILLE AND VICINITY. 

Between Provo and Springville the lowland contiguous to Utah Lake extends to the Rio 
Grande Railroad, above which the surface rises at a steep grade to the base of the moun- 
tains. The lowland for the most part is marshy, and the line that separates flowing and 
nonflowing wells lies only a short distance east of the railroad. A low scarp, which appar- 
ently marks a Pleistocene fault, can be traced immediately west of the county road for a 
mile or more beyond the Utah County Infirmary toward Springville. Springs occur at 
the base of the scarp, and the large springs at the head of Spring Creek may be associated 
with faulting. A number of small lakes mark the presence of these springs, and Spring 
Creek, whose main supply is thus derived, flows about 1,600 second-feet. 

The deepest well in this area is that of the infirmary, situated near the road about mid- 
way between Provo and Springville. The well is 3 inches in diameter and 270 feet deep, 
and water is reported to rise in a pipe to a point 3 feet above the surface, flowing about 30 
gallons a minute. In this vicinity a feeble first flow is reported at depths of 65 to 80 feet. 

Springville is situated on the plain about 3 miles below the mouth of Hobble Creek Can- 
yon, the channel of the creek passing through the town. During the irrigation season 
practically all of Hobble Creek water is diverted by canals that head near the base of the 
mountains. 

Ground water in Springville is obtained from wells that usually range in depth from 20 
to 30 feet, the water occurring in the top gravel. The general level of ground water in the 
town is reported not to have changed since the early days, and only an annual difference 
of a few feet is noticed between winter and summer conditions. a 

aStevenson, J. B., well driver. 



OCCURRENCE OF UNDERGROUND WATER. 53 

Records of wells in the vicinity of Springville show rather uniform conditions. The town 
generally is underlain by gravel 5 to 40 feet thick, below which blue clay occurs to a 
depth of about 130 feet, underlain by sand and gravel down to 180 feet; then about 50 
feet of light-colored clay is encountered, followed by sand and gravel at a depth of about 
230 feet. In the area nearer the lake the top gravel generally is wanting, but otherwise 
similar sections are reported in that locality. 

Flowing wells are obtained from the two lower gravel horizons at depths of approxi- 
mately 130 and 230 feet. The common occurrence of water at these two horizons implies 
unusual uniformity of underground conditions, and suggests a low lakeward dip, approxi- 
mately corresponding to the surface inclination. The wells are commonly 2 inches in diam- 
eter, though a few are 3 inches, and they yield on an average possibly 20 to 50 gallons a 
minute. One of the best in Springville is a 3-inch well belonging to A. Cox. It is 230 feet 
deep, flows about 120 gallons a minute, and its water is reported to rise in a pipe to a point 
18 feet above the surface. The Rio Grande Railway Company has two wells in Spring- 
ville, which are 216 and 304 feet deep. In the deeper the first flow was struck at 126 feet, 
a second at 216, a third at 260, and a fourth at 292. The shallower well is 3 inches in diam- 
eter, and is reported to flow about 200 gallons a minute at the surface, which is reduced to 
about 12 gallons a minute at the top of a tank about 30 feet above the surface. 

Mapleton Bench is the local name for the Provo Delta, lying between Spanish Fork and 
Hobble Creek. The delta is here prominently developed, and constitutes valuable farm- 
ing land. Flowing wells are not obtained on Mapleton Bench because of its elevation, but 
there are a number of dug wells. It is reported that in the early days the wells on the 
bench were 60 feet or more in depth, but since irrigation has been practiced the ground- 
water level has been considerably raised, and now the wells average possibly only 30 feet 
in depth. There is a- marked difl'erence in the depth to ground water in winter and sum- 
mer, the range in some instances amounting to over 10 feet. Along the outer margin of 
the bench there is a line of springs, many of which did not exist before the ditches were 
dug. Big Hollow Creek, a stream that flows from the bench about 2 miles south of Spring- 
ville, is a conspicuous example. In the early days scarcely an}^ water is said to have 
flowed in its channel, whereas it now irrigates over 100 acres. 

Considerable amounts of water are obtained by a few tunnels that have been dug along 
the eastern edge of Mapleton Bench. The entrances to the tunnels are commonly at the 
sites of springs. Some begin and end in unconsolidated materials, while others penetrate 
bed rock. The longest noted is in sec. 24, T. 8 S., R. 3 E. Its length i^ 275 feet. Water 
enough to irrigate about 100 acres comes through crevices in bed rock. 

SPANISH FORK, PAYSON, AND VICINITY. 

The town of Spanish Fork is situated on the general lowland at the base of Mapleton 
Bench and immediately north of Spanish Fork, about 5 miles- below the mouth of its 
canyon. From the few well records available it appears that sand and gravel com- 
monly underlie the surface to a depth of about 30 feet and are succeeded by 150 feet of 
clay, below which water-bearing gravel is usually encountered at a depth of 180 feet. The 
log of the well recently completed at the San Pedrd' station, about a mile west of the town, 
shows a greater thickness of clay, amounting to 205 feet, beneath which sand and clay were 
found to 390 feet, where water-bearing gravel occurs. 

Spanish Fork is rather poorly supplied with underground water. Dug wells commonly 
reach water at depths ranging from 10 to 25 feet, but its quality is not good. Flowing 
wells were formerly obtained, but in recent years the flows generally have ceased and pump- 
ing has to be resorted to. A city waterworks system was installed in 1904, the supply 
being derived from Evans Spring, near the mouth of Spanish Fork Canyon, about 5 miles 
above the towm, and an excellent supply is now available. The line separating flowing 
and nonflowing wells now lies in the extreme northwest corner of the town. The fii-st flow 
occurs at a depth of about 180 feet and a second flow between 350 and 400 feet. The cream- 
ery well, 2 iuchei in diameter and 220 feet deep, is typical. Water was struck at 180 feet 



54 UNDERGEOUND WATER IN VALLEYS OF UTAH. 

which in 1900 flowed 9 gallons a minute, while iii 1904 it stood about 4 feet below the 
surface with little or no variation. In 1904 the San Pedro, Los Angeles and Salt Lake 
Railroad Company put down a well 415 feet deep at its Spanish Fork -station and obtained 
a flow of 36 gallons a minute through a 2-inch pipe from gravel in the bottom of the well. 

Between Spanish Fork and the Goshen divide there are a number of settlements that 
are adjacent to the line separating flowing and nonflowing wells. 

Salem is situated at the lower end of the Provo Bench, about midway between Spanish 
Fork and Payson. In the northwestern part of the town the water table lies close to the sur- 
face and throughout the greater part of the settlement water can be obtained within 10 feet of 
the surface. There are many springs, the most important of which supply Salem Pond, which 
covers about 13 acres and averages possibly 12 feet in depth. The line separating flowing 
and nonflowing wells passes about midway through Salem. The flowing wells are gen- 
erally feeble and the quality of the water is poor. A first flow is commonly obtained at 
about 160 feet and a second at about 250 feet. 

Payson is situated on and near the delta formed by Peteneet Creek at the Provo stage 
of Lake Bonneville, part of the town being built on the delta and part on the subjacent 
plain. Flowing wells are not obtainable because of the elevation, and the underground 
water supply is furnished by dug wells. These vary considerably in depth because of the 
irregular distribution of the delta deposits. Their depth ranges from 15 to 115 feet and 
probably averages between 30 and 40 feet. As an instance of local variation it may be 
mentioned that in one well ground water is obtained at 18 feet while on the opposite side 
of the street a well was dug 90 feet without encountering water. The level of ground 
water is reported to fluctuate but little. A number of families in Payson are supplied by 
pipe lines, the water being derived from tunnels driven into the base of the bench. 

The town of Spring Lake is situated near the base of the mountains. The line separating 
flowing and nonflowing wells passes along the foot of the Provo Bench and lies about half 
a mile west of the town. In this locality ground water is found commonly within 10 feet 
of the surface and there are a number of shallow w^ells, but the chief supply comes from 
springs. Spring Lake covers an area of about 12 acres and discharges a stream of about 
2 second-feet. It is made by damming a small creek that is fed by springs. Springs occur in 
the vicinity of the base of the mountains between Spanish Fork and Spring Lake. Most of 
them appear to be seep springs, but some that lie near faults that adjoin the base of the 
mountains may be of deeper seated origin. Many of the springs flow 20 to 50 gallons a minute. 

Santaquin is built on a delta of Santaquin Creek, near the base of the mountains, far 
above the general level at which flowing wells are obtained. The town is chiefly supplied 
with water for both household and irrigation uses by Santaquin Creek, and only a few 
wells have been dug. About a dozen wells strike water in gravel at depths of between 15 
and 25 feet on a low bench in the southeastern part of the town. Tunnels are also dug into 
this bench, from which two pipe lines supply a number of families with water. Below the 
bench in Santaquin there are very few wells; two had to be dug about 80 feet before water 
was obtained. 

Below the line separating flowing and nonflowing wells between Hobble and Santaquin 
creeks the valley plain slopes gently to Utah Lake. Throughout this area ground water 
lies within 10 feet of the surface, and adjacent to the lake and in certain isolated localities 
swampy conditions occur. This area is mostly underlain by clay, which is reported to 
predominate in all of the wefls. Little or no gravel is encountered in well driving and the 
layers of clay alternate with layers of sand. Few satisfactory well records from this 
region have been obtained, and no correlation of the underground deposits has been possi- 
ble. Different conditions seem to exist in neighboring wells, indicating a lenticular arrange- 
ment of the deposits. 

The towns of Palmyra, Lake Shore, and Benjamin are situated below the line of flowing 
wells. Many farms are scattered over this area, but in a few localities — north of Spanish 
Fork, for instance — alkali is so prevalent as to discourage settlement. Much of the water 
used in irrigating this tract is derived from canals supplied by Spanish Fork, but flowing 
wells also are used to a considerable extent. 



OCCURRENCE OF UNDERGROUND WATER. 55 

Flowing wells have been obtained throughout this area at depths of 50 to 5(J0 feet, as 
shown by the list. Flows are usually found in every considerable bed of sand encountered 
in drilling, and six or more water-bearing beds are sometinus struck in a 40()-foot well. 
Shallow wells are not the rule in this i-egion, for, though many are 150 to 200 feet deep, the 
majority are nearer 400 feet deep. Because of the general absence of gravel and of persi.st- 
ent beds of sand there are few especially good wells. The flows obtained are generally 
under 50 gallons a minute and frequently are less than 10. The pressure is low, seldom 
being sufficient to cause the water to rise more than a few feet above the surface. 

At the southern end of the lake, north of West Mountain, just above low-water level 
there is a warm spring that was estimated to flow 200 gallons a minute. Its temperature 
is 88°. 

GOSHEN VALLEY. 

Goshen Valley can be divided into a highland and a lowland portion, a convenient line 
of division for present purposes being that which separates areas where ground water lies 
above 10 feet from the surface, from those in which it lies below that depth. The high- 
land lies contiguous to the mountains and merges into the lowland which adjoins the lower 
course of Currant Creek and the southern extremity of Utah Lake. The lowland is chiefly 
underlain by clay and the soils contain abundant alkali. a Throughout the entire area 
ground water lies close to the surface and marshy conditions exist, especially toward the 
lake. 

The area of flowing v/ells in Goshen Valley embraces about 15 square miles and extends 
from Utah Lake to within about a mile of Goshen. Within it flowing wells are obtained 
at depths ranging from 50 to 400 feet. From the few available records it appears that 
varying stratigraphic conditions exist in this area, the prevailing clay being irregularly 
interbedded with sand, usually in thin streaks, with very little gravel. The flows obtained 
are small, averaging possibly about 5 gallons a minute, and the pressure is sufficient to 
cause the water to rise only a few feet above the surface. 

Goshen itself is furnished with surface water from ditches supplied by Currant Creek and 
by springs located at the base of the hills about 2 miles east of the town. The underground 
supply is derived from wells that usually range from 25 to 75 feet in depth. The wells 
are put down through clay to sand in which water is found under pressure sufficient to 
cause it to rise almost to the surface, the usual depth to water being 3 to 20 feet. A 
number of unsuccessful attempts to get flowing wells have been made, the deepest being 
the railroad well put down near the station. It is 334 feet deep, and water is reported to 
have ri.sen in it to within a few feet of the surface. 

The highland area is underlain chiefly by coarse detritus derived from the adjacent 
mountains and distributed either as shore deposits in Lake Bonneville or as alluvial accumu- 
lations. This higher portion of Goshen Valley is poorly supplied with water, the chief 
sources being Kimball Creek, a small stream which seldom flows below its mountain course, 
and Currant Creek, which flows perennially and supplies the lower valley. The discharge 
of Currant Creek, however, is insufficient for the ne^ds of the upland. A reservoir has been 
built by damming Currant Creek at the entrance to its canyon course through Long Ridge, 
and a canal constructed which skirts the upper part of Goshen Valley, but the (enterprise 
has been a failure. 

A few springs occur along the eastern base of the Tintic Mountains and some successful 
attempts have been made there to develop underground water by tunneling. In the upper 
valley of Kimball Creek there are a number of springs which flow about 100 gallons a minute, 
and smaller ones o:'cur in several gulches. About 2 miles east of Goshen there is a group 
of springs at the base of Long Ridge, where water issues through debris and accumulates 
in several small ponds, the temperature of which is reported to stay at about 70° F. through- 
out the year. These springs constitute the source of Warm Creek, and their comi)ined 
flow in November, HK)4, was estimated at about 5 second-feet. Water has been devclopcnl 



o Sanchez, A. M., Soil survey of the Provo area, Utah: Bull. Bureau of Soils, U. S. Dept. Agric, 
1904. 



56 Ul^BERGROUND WATER IN VALLEYS OF UTAH. 

by tunneling at several localities along the eastern slope of the Tintic Mountains. In the 
valley of Kimball Creek, in sec. 11, T. 11 S., R. 2 W., there is a tunnel 200 feet long in vol- 
canic rock, which furnishes about 20 gallons a minute, and water sufficient for milling 
purposes has been developed by drifting into the alluvium and bed rock at the head of 
Homansville Canyon. a 

Away from the bordering mountains in the highland portion of Goshen Valley, very 
little underground water has been obtained, and considering the slight run-off and the small 
tributary drainage area, not much can be expected. The most favorable locations for sink- 
ing wells are along the courses of drainage ways. The most successful are along the course 
of Kimball Creek, but even there water commonly is not obtained at depths less than 150 
feet. A number of dry wells have been sunk in the upland area. 

WEST OF UTAH LAKE. 

The narrow strip of lowland between the western shore of Utah Lake and the Lake Moun- 
tains is very scantily provided with water. The low, narrow mountains catch relatively 
little precipitation; there are no perennial streams, and the arroyos carry water only for 
a few days during the year. From the foot of the Bonneville and Provo terraces that 
extend along the base of the mountains the surface slopes gradually lakeward and is under- 
lain chiefly by coarse-textured deposits. 

Along the shore of the lake a number of seep springs occur near water level. They are most 
abundant from Lehi southward, and there are also a few 2 or 3 miles beyond Pelican Point, 
where their presence is marked by low, marshy areas, one of which is utilized in the culti- 
vation of a few acres of alfalfa. Near Pelican Point there is a feebly flowing well 90 feet 
deep, in which water was obtained at a depth of 60 feet ; and in a near-by well a feeble flow 
is also obtained, which is said to come from a depth of 154 feet. 

Few if any other attempts have been made to r.ecover underground water in this region. 
Judging from the wells at Pelican Point one might expect to obtain similar results along 
the western shore of the lake, but if flows were obtained the water would be at so low an 
elevation as to make it of little use without pumping. Away from the shore flows can 
hardly be expected. It may be, however, that limited amounts of water can be found to 
rise in wells to within pumping distance. Prospecting for shallow wells might be attempted 
in the arroyos, but because of the limited watershed and precipitation the prospect is not 
good for obtaining enough underground water for extensive irrigation. Pumping directly 
from the lake presents attractive possibilities. 

>VELI. DATA. 

The writer is indebted for the subjoined list of wells to Messrs. F. D. Pyle and T. F. 
McDonald. Mr. Pyle worked in Utah Lake Valley and west of Jordan River. Mr. Mc- 
Donald, whose assistance was obtained through the courtesy of Mr. George W. Snow, 
engineer of Salt Lake City, collected data east of Jordan River. The yield of flowing wells 
was commonly measured by means of tables which are here inserted, together with accom- 
panying explanation, because the method aroused popular interest and because the edi- 
tion of the bulletin in which the tables were published has been exhausted. 

METHOD OF MEASUREMENT. 6 

Tables for determining the discharge of water from completely filled vertical and horizontal pipes 
were prepared a number of years ago by Prof. J, E. Todd, State geologist of Souih Dakota, who issued 
a private bulletin describing simple methods of determining quickly, with fair accuracy and with little 
trouble, the yield of artesian wells. In the following notes the tables and explanations relating to 
vertical and horizontal pipes are taken from this bulletin. The explanations have been appended by 
the present writer. 

a Smith, G. 0., and Tower, G. W., Description of the Tintic district: U. S. Geologic Atlas, special 
foUo 65, U. S. Geol. Survey, 1900. 
6 Slichter, C. S.: Water-Sup. and Irr. Paper No. 110, U. S. Geol. Survey, 1905, pp. 37-42. 



WELL DATA MEASUREMENT. 



57 



In determining the flow of water discharged through a pipe of uniform diameter all that is necessarj' 
is a foot rule, still air, and care in taking measurements. Two methods are proposed— one for pipes 
discharging vertically, which is particularly applicable before the well is permanently finished, and 
one for horizontal discharge, which is the most usual way of finishing a well. 

The table [on page 58] is adapted to wells of moderate size, as well as to large wells. In case the well 
is of other diameter than given in the table its discharge can without much difficulty be obtained from 
the table Ijy remembering that, other things being equal, the discharge varies as the square of the 
diameter of the pipe. If, lo • example, the pipe is one-half inch in diameter its dischar[ e will be one- 
fourth of that of a pipe 1 i:ich in diameter for a stream of the same height. In a similar manner the 
discharge of a pipe 8 inches in diameter can be obtained In' multiplying the discharge of the 4-inch 
pipe by 4. 

In the first method the inside diameter of the pipe should first l;e measured, then the distance from 
the end of the pipe to the highest point of the dome of the water above in a strictly vertical direction — 
a to b in the diagram [fig. 5]. Find these distances in table [p. 58, A] and the corresponding figure will 
pive the number of gallons discharged each minute. Wind would not interfere in this case so long as 
the measurements are taken vertically. 

The method for determining the discharge of horizontal pipes requires a little more care. First meas- 
ure the diameter of the pipe, as before, then the vertical distance from the center of the opening of the 
pipe, or some convenient point corresponding to it on the side of the pipe, vertically downward G inches, 
a to 6 of the diagi'am, then from this point strictly horizontally to the center of the stream, b to e. 





Illil 
Fig. 5.— Diagram illustrating flow from vertical and horizontal pipes. 






With these data the flow in gallons per minute can be obtained from table [p. 58, B]. It will readily be 
seen that a slight error may make much difference in the discharge. Care must be taken to measure 
horizontally and also to the center of the stream. Because of this difficulty it is desirable to check 
the first determination by a second. For this purpose columns are given in the tables for corresponding 
measurements 12 inches below the center of the pipe. Of course the discharge from the same pipe should 
be the same in the two measurements of the same stream. Wind blowing either with or against th(> 
water may vitiate i-esults to an indefinite amount. Therefore measurements should b(^ taken while 
the air is still. 

Whenever fractions occur in the height or horizontal distance of the stream, the number of gallons 
can be obtained by apportioning the difference between the readings in the table for the nearest whole 
numbers, according to the size of the fraction. For example, if the distance from the top of the pipe 
to the top of the stream in the first case is 9J inches, one-third of the difference between the reading in 
the table for 9 and 10 inches must be added to the former to give the correct result. 

In case one measures the flow of a well by both methods he may think that the results should agree, 
but such is not the case. In the vertical discharge, there being less friction, the flow will lie larger; so, 
also, in the second method differences will be found according to the length of the horizontal pipe used. 

As pipes are occasionally at an angle, it is well to know that the second method can hv applied to 
them if the first measurement is taken strictly vertically from the center of the opening and the second 
measurement from that point parallel with the axis of the pipe to the center of the stream, as before. 
The measurements can then be read from the table. 



58 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



Table for determining yield of artesian wells. 
[Gallons per minute.] 



A. — Flow from vertical pipes. 


B. — Flow from horizontal pipes. 






Diameter of pipe 


in inches. 


Hori- 


1-inch pipe. 


2-inch pipe. | 


Height 
of jet. 












zontal 
leigth 
of jet. 










1. 


l\- 


IJ. 


2. 


3. 


6-inch 
level. 


12-inch 
level. 


6-inch 
level. 


12-inch 
level. 


Inches. 












Inches. 










i 


3.96 


6.2 


8.91 


15.8 


35.6 


6 


7.01 


4.95 


27.71 


19.63 


1 


5.60 


8.7 


12.6 


22.4 


51.4 


7 


8.18 


5.77 


32.33 


22.90 


2 


7.99 


12.5 


18.0 


32.0 


71.9 


8 


9.35 


6.60 


36.94 


26.18 


3 


9.81 


15.3 


22.1 


39.2 


88^3 


9 


10.51 


7.42 


41.56 


29.45 


4 


. 11.33 


17.7 


25.5 


45.3 


102.0 


10 


11.68 


8.25. 


46.18 


32.72 


5 


12.68 


19.8 


28.5 


50.7 


113.8 


11 


12.85 


9.08 


50.80 


35.99 


6 


13.88 


21.7 


31.2 


55.5 


124.9 


12 


14.02 


9.91 


55.42 


39.26 


7 


14.96 


23.6 


33.7 


59.8 


134.9 


13 


15.19 


10.73 


60.03 


42.54 


8 


16.00 


25.1 


36.0 


64.0 


144.1 


14 


16.36 


11.56 


64.65 


45.81 


9 


17.01 


26.6 


38.3 


68.0 


153.1 


15 


17.53 


12.38 


69.27 


49.08 


10 


17.93 


28.1 


40.3 


71.6 


161.3 


16 


18.70 


13.21 


73.89 


52.35 


11 


18.80 


29.5 


42.3 


75.2 


169.3 


17 


19.87 


14.04 


78.51 


55.62 


12 


19.65 


30.7 


44.2 


78.6 


176.9 


18 21.04 


14.86 


83.12 


58.90 


13 


20.46 


31.8 


45.9 


81.8 


184.1 


19 22.21 


15.69 


87.74 


62.17 


14 


21.22 


33.0 


47.6 


84.9 


190.9 


20 23.37 


16.51 


92.36 


65.44 


15 


21.95 


34.2 


49.3 


87.8 


197.5 


21 24.54 


17.34 


96.98 


68.71 


16 


22.67 


35.2 


50.9 


90.7 


203.9 


22 / 25.71 


18.17 


101.60 


71.98 


17 


23.37 


36.3 


52.5 


93.5 


210.3 


23 \ 26.88 


18.99 


106.21 


75.26 


18 


24.06 


37.5 


54.1 


96.2 


216.5 


24 28.04 


19.82 


110.83 


78.53 


19 


24.72 


38.6 


55.6 


98.9 


222.5 


25 29.11 


20.64 


115.45 


81.80 


20 


25.37 


39.6 


57.0 


101.6 


228.5 


26 , 30.38 


21.47 


120.07 


85.07 


21 


26.02 


40.6 


58.4 


104.2 


234.3 


27 31.55 


22.29 


124.69 


88.34 


22 


26.66 


41.6 


59.9 


106.7 


240.0 


28 ' 32.72 


23.12 


129.30 


91.62 


23 


27.28 


42.6 


61.4 


109.2 


245.6 


29 33.89 


23.95 


133.92 


94.89 


24 


27.90 


43.5 


62.8 


111.6 


251.1 


30 35.06 


24.77 


138.54 


98.16 


25 


28.49 


44.4 


64.1 


114.0 


256.4 


31 36.23 


25.59 


143.16 


101.43 


26 


29.05 


45.3 


65.3 


116.2 


261.4 


32 37.40 


26.42 


147.78 


104.70 


27 


29.59 


46.1 


66.4 


118.2 


266.1 


33 38.57 


27.25 


152.39 


107.98 


28 


30.08 


46.9 


67.5 


120.3 


270.4 


34 


39.64 


28.08 


157.01 


111.25 


29 


30.55 


47.5 


68.5 


121.9 


- 274.1 


35 


40.45 


28.64 


161.63 


114.52 


30 


30.94 


48.2 


69.4 


123.4 


277.6 


36 


41.60 


29.46 


166.25 


117.79 


36 
48 
60 


34.1 
39.1 
43.8 


53.2 
61.0 
68.4 


76.7 
88.0 
98.6 


136.3 
156.5 
175.2 


306.6 
352.1 
394.3 


Continue by a 
: 1.15 


dding fc 
0.82 


r each i 
4.62 


nch— 
3.27 


72 


48.2 


75.2 


108.0 


192.9 


434.0 










84 


51.9 


81.0 


116.8 


207.6 


467.0 










96 


55.6 


86.7 


125.0 


222.2 


500.0 










108 


58.9 


92.0 


132.6 


235.9 


530.8 










120 


62.2 


98.0 


139.9 


248.7 


559.5 










132 


65.1 


102.6, 


146.5 


260.4 


585.9 










144 


68.0 


106.4 


153.1 


272.2 


612.5 











Note.— To convert results into cubic feet, divide the number of gallons by 7.5, or, more accurately, 
by 7.48. 

The flow in pipes of diameters not given in the table can easily be obtained in the following manner: 

For |-inch pipe, multiply discharge of 1-inch pipe by 0. 25 

For |-inch pipe, multiply discharge of 1-inch pipe by 56 

For 1 J-inch pipe, multiply discharge of 1-inch pipe by 1-56 

For 1 J-inch pipe, multiply discharge of 1-inch pipe by 2. 25 

For 3-inch pipe, multiply discharge of 2-inch pipe by 2. 25 



LIST OF TYPICAL WELLS. 



59 



For 4-inch pipe, multiply discharge of 2-inch pipe by 4. 00 

For 4.i-iiich pipe, multiply discharge of 2-inch pipe by o.OO 

For 5-inch pipe, multiply discharge of 2-inch pipe by <>. 25 

For f)-inch pipo, multiply discharge of 2-inch pipe l)y 9.00 

For 8-inch pipe, multiply discharge of 2-inch pipe l)y Itj. 00 

LIST OF TYPICAL WELLS. 

Wells in Jordan River and Utah Lake valleys. 

[Height of water above surface indicated by t)lus + ; below surface indicated by minus — .] 



Name of owner. 



B. Young 

J. L. Haywood 

R. R. Anderson 

C. R. Savage 

G. A. Hatch 

J . Howard 

Stockyards 

T. German 

F. S. Rudy 

J. E. Peterson 

J. Minegar 

Do 

R. A. Bosley 

J. C. Hansen 

W. S. McDonald 

Gun Club 

J. Herridge 

G. Baldwin 

C. A. Anderson 

P. Olene 

S. Bamberger 

G. Fritt 

J. Withers 

I. Langton 

G. Martin 

A. J. Davis 

F.W. Kettle 

A. M. Davis 

Do 

E. King 

Wantland 

J. J. Sears 

Do 

Do 

P. Cline 

R. Weisner 

J. W. Evans 

W. Pearson 

J. W. Haddock 

A.Elkins 

A. J. Ridges 

W. Spicer 

J. Sandborg 

H. Price 

Mrs. Winters 

R.Griffith 



Location. 



T. 1N..R.1 E., sec. 31 

....do 

....do 

T. IN., R. IE., sec. 32 

T. 1 N., R. 1 W., sec. 1 

....do 

T. IN., R. 1 W., sec. 3 

T. 1 N., R. 1 W., sec. 4 

T. 1 N., R. 1 W., sec. 5 

T. 1 N., R. 1 W., sec. 9. 

T. 1 N., R. 1 W., sec. 10 

....do 

T. 1 N., R. 1 W., sec. 11 

T. 1 N., R. 1 W., sec. 15 

T. 1 N., R. 1 W., sec. 17 

T. 1 N., R. 1 W., sec. 21 

T. 1 N., R. 1 W., sec. 22 

do 

T. 1 N., R. 1 W., sec. 23 

do 

T. 1 N., R. 1 W., sec. 25 

.^..do 

do.. 

T. 1-N., R. 1 W., sec. 2G 

do 

T. IN., R. 1 W., sec. 27 

do 

T. 1 N., R. 1 W., sec. 34 

do 

do 

do 

T. 1 N., R. 1 W., sec. 35 

do 

do 

do 



.do. 



.do. 



T. 1 N., R. 1 W., sec. 36. 
do 



.do. 
.do. 
.do. 
.do. 
.do, 
.do. 
.do. 



Diame- 
ter. 



Inches. 



Depth. 



1,002 

497 

150 

250 

50 

479 

400 

450 

160 

330 

28 

26 

60-70 

80 

70 

400 

140 

154 

208 

408 

250 

320 

350 

140 

210 

350 

135 

1.30 

08 

93 

95 

123 

100 

75 

75 

75 

96 

200 



Height of Yield per 
water. , minute. 



Feet. Feet. 

75 
61 



35 

18 

312 



GaUon.s 



-20-50 



-I- 
+ 
+ 
-I- 
+ 1 



Many. 
6 



40 

30 

3-7 

3 



3 

1-2 

1 



25 

1 

1 



5 

15 

2 

3 

2 

15 

85 

30 

25 

5-20 



60 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



Wells in Jordan River and Utah Lake valleys — Continued. 



Name of owner. 


Location. 


Diame- 
ter. 


Depth. 


Height of 
water. 


Yield per 
minute. 


S. A. Gibbs 


T. IN., R. 1 W.,sec. 36 

T. 1 N., R. 2 W., sec. 25 


Inches. 
2-3 


Feet. 

75-80 

400 

401 

465 


Feet. 

+ 


Gallons. 
40 


F. Auerbach 




J. Bond 


T. 1 N., R. 2 W., sec. 29 




+ 

+ ■ 
+ 
+ 

- 6 

-12 

- 6 

- 

+ 
+ 

+ 

+ 

+ 

+ 

+ 

+ 

+35 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

- 1 
+ 

+ 
+ 
+ 12 

-5-6 

• -65 
-30-50 

-46 

- 4-16 

- 5-14 

+ 
+ 

- 3-11 

- 3 


4 


Do ' .. 


.do... . 




9 


Ciillen Dairy 

J. Walker 


T. 1 N, R. 2.W., sec. 35 


2 




T. 1 S., R. 1 E., sec 5 


80 

16 

73 

45 

29 

40 

12 

75 

82 

387 

10 

100 

162 

100 

125 

170 

150 

100-600 

178 

150-200 

155 

160 

60 

165 

110 

50 

- 50 

26 

246 

390 

207 

41 

28 

42 

100 

130 

85 

51 

54 

56 

18 

32 

22 

20 

100 

200 

335 

15 

33 


20 


P. J. Stone 


do... 




J. Lunn 


do 






W. J. Kelson 


do 






S. McKay 


do 






Speirs 


do 






Do 


do 






J. E. Wesley.. 


T. 1 S., R. 1 E., sec. 6 








do 


2 
2 


7 


H. S. Sampson 


do 


8 


W. Wheeler. . 


do 




T. Golightly 


.do 


2 
2 
2 




S. K: Hansen 


do 


6-8 


W. N. Sheets 


T. 1 S., R. 1 E., sec. 7 


30 


F. Sproul 


.do 


^ 


G. Baiber 


do 


12 


F. Rogansky 


do 




1 


City, about 16 wells . . . 
E. 0. Butterfield 


do 

.do 


2-9 
2 


(?) 600 
2-3 


J. S.Wooley and others 


do 


20-50 


T. Berg 


do .. 


2 
2 
2 
2 
2 

li 

2 

3 

2 

IJ 

2 


50 


Do 


. .do 


50 


W. Colton 


. ...do 


6 


L. Badger. 


do 


30 


J. W. Hicks. .. 


. .do 


35 


A. Duncan 


T. IS. R. 1 E., sec. 8 




T. Antisill... 


do 


3 


S.M. Alley 


. .do 




S. H. Calder 


do : 


40 


S. Sudbury... 


do . . 


8 


J.R.Miller 


...do 


50 


P. Rosmason 


do 






do ... 






W. Pickens 


do 


. 






T. 1 S., R. 1 E., sec. 9 






A S Martin 


T 1 S R 1 E sec 10 






J. A. Shelter 


T 1 S R 1 E sec. 15 






L. Hunt. . 


do 






A Hord 


T 1 S R 1 E sec 16 






A. Martin 


do 






H. E. Thorp. 


do 






J S. Southern 


T 1 S R 1 E sec. 17 








do 






J E Nailor 


do 






T. Y. Taylor 


do 


2 
2 
2 




(a) 


do 


6 


W H Miller 


do 


50 


W. H. Burnett . 


do 




M. C. Sandford 










a Owner's name unknown. 



LIST OF TYPICAL WELLS. 



61 



WeU.''i in Jordan River and Utah Lake valleys — Continued. 



Name of owner. 




Location. 


Diame- 
ter. 


Depth. 


Height of 
water. 


Yield per 
minute. 




T.IS. R. 

do... 

do 


1 E., sec. 17 



1 E., sec. 18 


Inches. 


2 
2 
2 
2 


Feet. 
33 
10 

14 

48 
325 
300 
100 
164 
160 

20 
72-82 
500 
600 
636 
150 

40 

325-3C0 

501 

382 

17 

250-300 

322 

560 

40 
298 

m 

50 
160-170 
323 
296 
285 
150 
437 
100 

94 

60 
176 
180 

90 
181 

84 
212 

75 
240 

150 
150-l(i0 
23 
20 
65 
40 
162 
156 
21 


Feet. 
-28 

-43 

+ 

+ 
+ 

+ 
+ 
4- 
+ 
+ 
+ 

+ 
+ 

+ 

+ 

+ 
+ 
+ 



+ 

+ 

+ 

+ 
+ 

+ 

+ 
+ 
+ 
+ 

+ 
+ 
4- 

-20 

4- 
4- 
4- 
-14-15 


Gallons. 


G Hemslev 








do 




J. J. Ilurtt 


T. 1 S., R 
do 


4-5 


T Furgesou 




30-40 


W N Sheets 


do 


30 


M. Gray 


.do 


10 


F II Woodbury 


do 


18 


M P Holmes 


do. 






E. H. Stout 


.do... 


!'^'!^^"^'^^!!!^!"'!!^ 


2 
2 
2 
2 
2 
2 
2 


30-40 


J. II. Cochran 


....do... 


5 


F. Prittish 


do 


12-14 


Salt Lake Co 


.do... 


(?j 150 




do... 


10 


F. Wittich 


do... 


18 


L. A. Kelsh 


.do... 


30-40 


D. Evans 


do... 


80 


Eriekson 


do... 





3 


(?) 100 


I. Riches 


.do... 






do... 




2 

2 


1-13 


E. S. Pierce 


do 


55 


(") 


. .do... 


20-30 


W. II. Wolstezhoh 


do... 

do 


1 E., sec. 19 


3 
2 
2 

n 

3 
2 

2 
2 
2 

2 
2 
2 
2 

2 

2 
2 
2 

2 

3 

2 




C. B. Stock 


10-12 




.do... 


5-6 


H. Best 


do... 


8 


A. Best. 


do 




J. A. Bush 


T. IS., R 
do... 




J.H. Tipton 


50-60 


L. W. Burton. . 


.do 


60 


Do 


.. ..do... 


25 


Do 


do 


lO-SO 


Do 


.do... 




J. Riley 


do... 


17-20 


G. JIall 


do 


1 


J. C. Ilogan 

J. 0. Young 

R. B. Young 

M. W. Taylor 

L. II. Kimball 

Do 

W. C. Winder 


do... 

do... 

do.. . 

do... 

do... 

do... 

do... 

':■■■ 

do... 

do... 


18 

20-25 

20-25 

(?)100 

10 

1 


Do 




A. Walker 

(«) 
E. P. Parrot 


30 
40 
46 


11. Behling 


T. 1 S.. R 
do... 


1 E., sec. 20 




H. Eldridge 




T. R. Cutler 


do 




S. Love 


do... 


5-6 


M. C. Morris 


do 


1 


N. .1. Hansen 

A. Uoskinson 


do... 

do... 


28 



a Owner's name unknown. 



62 



UNDEEGEOUND WATEE lis" VALLEYS OF UTAH. 



Wells in Jordan River and Utah Lake valleys — Continued. 



Name of owner. 


Location. 


Diame- 
ter. 


Depth. 


Height of 
water. 


Yield per 
minute. 


C. Hansen.. 


T. 1 S., R. 1 E., sec. 20 


Inches. 


Feet. 

22 

158 

18 

22 

23 

100 

33 

184 

27 

55 

68 

68 

26 

194 

187 

40 

260 

190 

200 

184 

215 

208 

209 

245 

245 

141-143 

100 

120 

202 

24 

200 

128 

251 

104 

235 

240 

110 

216 

218 

130 

100 


Feet. 

- 18 

+ 

- 19 

- 20 
-104 

- 25 

_ 

- 37 

+ 

- 34 
-16 

+ 
+ 

+ 

+ 
+ 
+ 
+ 
+ 
+ 
+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 6 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 
+ 

+ 


Gallons. 


P. E,. Ryon 


do 




80 


G. Cusiman 


do 






W. C. Smoot 


do 






J; Neff 


T. 1 S., R. 1 E., sec. 26 






C. Banford 


do 






J. Fisher 


T. 1 S., R. 1 E., sec. 27 








.. ..do 






F. Ereickson 


T. 1 S., R. 1 E., sec. 28 






J. Childs 


T. 1 S., R. 1 E., sec. 29 






W. M. Tillman 


do 






F. Degenhart 


do 


2 




J. P. Gaboon 


do 




W. S. Timmons 


. ..do 


2 
2 


9 


J. T. Guest 


do 




R. Pike 


do 






..do 






J. S. Gustavensen 


do 


2 


2 


H. Hizzard 


do 


2 


Mrs. C. Green 


..do 1 




Do 


do 




11 


S. F. Evans 


do 

.do 


,2 




0. Reece 


30 


Do 


do 




30 


Do 


do 




13 


L. Stutts 


. ..do : 


2 
2 
3 


40 


S. Hicks 


do 


30 


E. E. Keithley 

H. Burnett 


do 


(?) 100 


. .do 


27 


Do ' 


do 






W. J. Miller 


do 


2 
2 
2 


20 




. ..do 


20 


J. Tremayave 

G. Taylor 


T. 1 S., R. 1 E., sec. 30 


20 


.do . 




W. Chantron 

J J. Spencer 


do 

do 


2 
2 

2 

2 
2 

2 
2 
2 

2 


30 

17 


M. M. Listen. 


.do 


5 


J. Cobert 


do 


24 


Scbool 


do 


12 


G. Calder 


..do 


45 


R Norman 


do 




Mrs. A. S. Berg 


do 


28 




do 


175 


8 


(a) 

Murray Live Stock Co. 


do 


30 


.do 




40-6® 


:.;..do 


300 
185-230 
82-83 
50 
160 
202 
72 
237 
160 


20 


L. White 


do 




60 


E J Williams 


do 


2 

2 

li 

2 

2 

2 

2 


25 


Do 


do. 


1 


C. Halford 


.do 


10 


A. M. Rymarson 

Do 


T. 1 S., R. IE., sec. 31 

do . 


35 
6 


L Parks 


do 




J.Hulse 


do 


+ 


20 



a Owner's name unknown. 



LIST OF TYPICAL WELL8. 



63 



Wells in Jordan River and Utah Lake valleys — Continued. 



Name of owner. 




Location. 


Diame- 
ter. 


I)ei)th. 


Height of 
water. 


Yield per 
rninutc. 






Inches. 


Feet. 


Feet. 


Gallons. 


J. Hulse . ... . 


T. 


1 S., R. 1 E.,sec. .-^l 

do 


2 

2 


130 

255 
83 


+ 
4- 


20 


Do 


30 


J. Pearson 

C. Bell 


do 






..do 


2 


209 


+ 


40 


Do 




do 




211 
203 


+ 


20 


J. Bert 


..do 


2 


12 


C. Cramer 




..do 




1.50 


4- 


C!) 110 


Do 




.do 




90 


+ 




N. White 




..do 

..do 




i;30 

80 


4- 
+ 


15 


J. Anderson 




h 


S. Ilaslam 




..do 


2 


244 


-f 


8 


E. lluish 




1 S., R. 1 E., SfiC. 32 


2 


210 


+ 


28 


Do 




..do 




70 


+ 


35 


S. W. Moylo 




..do 




196 


+ 


6 


J. Cormvell 




..do 




235 


+ 


20 


Do 




..do 

..do 




lOO 
160 


+ 
+ 




Do 


1-12 


Do 




..do 


2 


165 
193 


+ 
+ 




S. A.Cornwpll 


1 


Do 




..do 


2 


55 


+ 




A. Young 




..do 




33 


- 24 




E. Bailey 




..do 




25 


- 22 




L. E. Sowers 




.do 




54-56 
70-150 


- 




J. \V. Murphy 

C. A. North 






1 S., R. 1 E. sec 33 




25 
520 


-419 




W. H.Thuers 


..do 


3 




P. C. Brizen 




..do 


3 


350 


+ 


25 


Mrs. M. Cold 




1S.,R. 1 W.,sec. 1 '. 


1^ 
2 


317 
300 


+ 
-f. 


1 


J. R. Morgan 

Mrs. E.R. Wadsen.... 


.do .- 


20 


T. 


..do 


2 
3 


202 

120 

1,100 


+ 


2 


(a) 


1 S., R. 1 W., sec. 2 




J. Harrison 


..do 


30 


F.J. Guth 




..do 


2 


114 


+ 


li 


Mrs. C. Bickson 




..do 


2 


318 


4- 


6 


J. H. Haward 




..do.: 


2 


335 


4- 


4 


J. Taylow 




..do 


1 


95 


4- 


2i 


Rio Grande Rwy 




..do 


4 


1,072 


+ 30 


80 


H. L. Eyler 

Mortensen 


T 

T. 


1 S., R. 1 W., sec. 3. 


2i 
2 


381 
280 


+ 

4- 


16 


IS., R 1 W.,sec. 4 


3 


R. Boss 


T. 


1 S., R. 1 W.,sec. 5., 


2 


360 


+ 4i 


7 


E. B Swan 




-do 


2 


38.5 


4- 


6 


J. Rodgers 


T. 


1S..R. 1 W.,sec. 7 

.do 


2 


154 
405 


4- 




Do 


10 


Do 


T. 


.do 

1 S., R 1 W.,sec. 8 


n 

2 


154 
325 


4- 
+ 1 




F. Schonfeld 


1 


Brighton School 


T. 


] S., R. 1 W., sec. [) 


2 


320 

98 


4- 
+ 1 


5-6 


11. J. Walk 


-do 


1 


H. E.Evans 


T. 


IS., R. 1 W.,sec. 10 


3 


624 


+ 


30-40 


W. Baden 


T. 


1 S., R. 1 W.,sec. 11 


2 


377 


4- 


9 


W. J. Kinsman 




.do 


2 


130 


+ 


20-30 


Cannon 




.do 




165 


+ 


6-7 


Sudbury 




.do 


2 
2 




4- 
+ 


25 


A. Bailey 


.do 


367-387 


5-6 


J.Cleveland 


... 


.do 


2 


456 


4- 


60-70 



a Owner's name unknown. 



64 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



Wells in Jordan River and Utah Lake faZZej/s— Continued. 



Name of owner. 



E.Kidd 

A.H.White 

J. Anderson 

J. H. Shaffer 

Lambert Paper Co . 

R. Cutler 

J. Gabbot. 

(a) 

J. S. McCallan 

J. G. Gumman 

Schoolhouse 

S. C. Sudbury 

L. S. Hansen. .. 

N. Hansen 

S. Sorensen 

Gilchrist 

Rockhill 

P. Austin 

G.H.Walton...... 

B. Harmon 

(a) 
Murray 

C. J. Lambert 

L. Burden 

N. P. Peterson 



J. C. Poulton 

(a) 

T. P. Jones 

Do 

(a) 

J. P. Anderson 

(a) 
(a) 

Wolstenholm 

Spencer 

Oslen 

Butterworth 

T. West 

N. T. West 

J. Michaels 

J. Hayhoe 

Goodwin 

A. Cockerill 

Speirs 

J. Kersey 

Inland Crystal Salt Co . 
Salt Lake and Los An- 
geles Rwy. Co. 

P. J. Reid 

J. Bertock 

J. Neilson 

G. Coleman 

T. Newman 

T. Gundesser, jr 



Location. 



R. 1 W. 
R. IW. 



sec. 26. 
sec. 28. 



T. 1 S., R. 1 W., sec. 12. 

do 

T. 1 S., R. 1 W.,sec.l3. 

do 

do 

do 

do 

do 

T. 1 S., R. 1 W.,sec. 14. 
T. 1 S., R. 1 W.,sec. 16. 
T. 1 S., R. 1 W., sec. 17. 
T. 1 S.,R. 1 W.,sec. 18. 
T. 1S.,R.1 W.,sec. 21. 
T. 1 S., R. 1 W., sec. 24. 

do 

T.1S.,R. 1 W., sec. 25. 

do 

do 

do 

T. IS., 
T. 1 S., 

do 

T. 1S.,R. 1 W., sec. 29. 

do 

T. 1 S.,R. 1 W., sec. 31. 

do „... 

T. 1S.,R. 1 W.,sec. 32. 
T. 1S.,R. 1 W.,sec. 35. 

do 

T. 1S.,R. 1 W.,sec. 36. 
T. 1S.,R. 2 W.,sec. 1.. 

do 

T. 1S.,R.2 W.,sec. 14. 
T. 1 S., R. 2 W.,sec. 21. 

do 

do 

do 

T. 1 S., 

do. 

T. IS., 
T. 1 S., 
T. IS., 
T. IS., 
T. IS., 
T. IS., 
T. IS., 
do. 



R. 2 W., sec. 22. 



R.2W., sec. 23... 
R.2W.,sec. 26... 
R. 2 W., sec. 27... 
R. 2 W., sec. 29... 
R.2 W.,sec. 33... 
R. 2 W., sec. 34... 
R. 3W.,sec. 2.... 



T. 1S.,R.3 W., sec. 24 

do 

T.2 S.,R. 1 E., sec. 3 

do 

.....do 

T. 2S., R. lE.,sec. 4 

a Owner's name unknown. 



Diame- 
ter. 



Inches. 



Depth. 



Feet. 
475 
300 
400 
18 
177 
315 
380 
275 
355 
330 
400 
412 



145 
385 
130 
120 
145 
350 
350 
290 



182 

70 

50 

60 

290 

345 

75 

140 

160 

260 

150 

30 

68 

150 

175 

40 

40 

90 

177 

27 

118 

84 

166 

720 

330 

134 
73 

540 
62 
65 
18 



Height of 

water. 



Feet. 



+ 3 
+ 6 
+ 

-21 
-14 

-66 
+ 9 
+ 12 



LIST OF TYPICAL WELLS. 



65 



Wells in Jordan River and Utah Lake valleys — Continued. 



Name of owner. 



Location. 



R. 1 E., sec. 5. 



R. 1 E., sec. 6. 



T. R. Brockbank T. 2 S., R. 1 E., sec. 4 

Do do 

J. Southerland do 

Do do 

Do do 

Do do 

W. Templeman do 

F. Hopp do 

A. Fuller do 

Do ' do 

P. C. Brizen ' do 

J. Wright T.2 S. 

E. Pugh ' do 

S. A. Williams do 

Mrs. A. D. Park do 

0. Lemon do 

H.J. Bullock T.2S. 

T . Powell do 

H. Park do 

W. Hill, sr do 

Do do 

W. Hill, jr do 

G. E. Christensen do 

J. Godfrey T.2 S., R. 1 E., sec. 7 

1. Hackley do 

Mrs. B. Erickson do 

J. S. Williams do 

E. Williams do 

Williams do 

Martin do 

Warenski ' do 

E. Warenski do 

R. Miller T. 2 S. 

W.Noble do 

M. M.Miller do 

Do do 



T. H. Pierce 

C. West 

J. Walker 

State fish hatchery . 

Do 

Do 

A. Gillard 

H. Brinton 

J. R. Hansen 

L. B. Howard 

A. Scott 

H. Bagley 

Do 

W. Reynolds 

F. Brinton 

C. Bagley 

Do 



do 

do 

do 

do 

do 

do 

do 

do 

T. 2S. 

do 

do 

do 

do 

do 

do 

do 

do 



R. 1 E., sec. 9 



R.Anderson T. 2 S., R. 



IRR 157—06- 



Diame- 
ter. 



Inches. 



Tv^^+v, Height of 
^«P*^- I witer. 



1 E., sec. 10 

a Drv 9 months in year. 



2 






, R. 1 E., sec. 8 




5 


2 







2 ! 



Feet. 
104 
102 
76 
78 



225 
70-100 

65 
335 
122 
200 
108 
180 

90 
384 
100 
194 

90 
255 

80 
255 
210 
150 
115 

80 
315 
100 
190 
189 
230 
300 
215 
230 

85 

82 

80 
172 

80 



310 



120 
148 



2 I 275-250 



100-103 

92-96 

100 



14 



Feet. 

+ 
+ 
+ 
+ 
+ 



Yield per 
minute. 



Gallons. 



+ 


30 


+ 


15 


+ 


4 


+ 


10 


+ 


38 


+ 




+ 


2 



(«) 



66 



UNDERGROUND WATER IN VA.LLEYS OF UTAH. 



Wells in Jordan River and Utah Lalce valleys — Continued. 



Name of owner. 


Location. 


Diame- 
ter. 


Depth. 


Height of 
water. 


Yield per 
minute. 


A. Olander 


T. 2 S., R. 1 E., sec. 15 


Inches. 


Feet. 
18 
15 
20 
78 
18-20 
20 
22 
18 

113 
60 
60 
92 
58 
83 
14 

250 
40 
46 
50-60 
60 
45 

175 
90 

190 
75 
80 

125 

20-30 

90 

70-80 

200 

22 

75-100 

75-100 

110 
18 
50 
22 
10 
12 
22 
10 
16 
13 
50 
6 

12 
80 
96 

125 
18 
22 
35 


Feet. 

- 16 

- 10-11 

- 4-17 

- 40 

- 8-10 

- 10 

- 11 

- 12 

- 9 
+ 

+ 

+ 16 
+ 8 . 

- 9 

- 12 

+ 8 

+ 
+ 

+ 
+ 
+ 
+ 
+ 
+ 
-117 

- 10 

- 4-13 

- 10 

+ 
+ 

+ 

- 4 

- 8 

- 30 

- 55 

- 93 

- 


Gallons. 


J.Sioiilet 


.. .do ..' 




J. Smith 


T. 2 S., R. 1 E., sec. 16 ' 




J. Hemmert 


do 


- 




S. Neilson 


.. .do 




S. F. Smith 


do 




A. L. Hansen 


do 




J. W. McHenry 


.....do ' 




J. Hobbs 


do 






J. Furgeson 


do 




17 


I . Furgeson 


do 








do 






J. Brighouse 

H.V.Ballard. 


T.2S., R. IE., sec. 17 

.do 


li 
2 


30 
50 




do 




District school 


do 






R. Brown 


.do. .. ^ 






R. M. Ballard.. 


do 


li 
2 


35 


Mrs. Shumann 


do 


20 


H. E. Howe 


do .. . 


22 


D. A. Rauser. 


do.. 


.. 


60 


J. T. Erickson 


do 


2 
2 
2 
li 
2 


2 


F. C. Howe 


do 


35 


Do 


do 


35 


J. B. Thompson 

Do 


do 


45 


do 


60 


E. Taylor 

E. Gillen 


T 2 S., R. 1 E., sec. 18' 




...do 


2 
3 




H. Berger 


do 




C. Turner 


do . 






...do 


2 
2 
2 

2 

3 




J Jones 


do 




J. H. Wheeler 


.do.. . 


20 


South Cottonwood 


do . . 


40 


Ward. 
Do. 


do 


60 


Mrs. J. Clark 


do... 




M. Sibbs 


T. 2 S., R. 1 E., sec. 19 


2 






... .do 






T. 2 S., R. 1 E., sec. 20 






H. Wheeler 


do. ... 






C. B. Walder.. 


do 






C. J. Wright 


do 






W. Barrett 


T. 2 S., R. 1 E., sec. 21. 






J. E. Brown... 


do. 






H. C. L. Russell 


do 






J. W. Fawlke 


T. 2 S., R. 1 E., sec. 22 






A. Fawlke 


do 






S. Jones 


T. 2 S., R. 1 E., sec. 26 






A. D. Brown 


T. 2 S., R. 1 E., sec. 27 






(a) 

W. Baggas. . 


T. 2 S., R. 1 E., sec. 28 






T. 2 S., R. 1 E., sec. 29 






D. M. Griffin 


do 






J. A. Wagstaff 


do : 







■ Owner's name unknown. 



LIST OF TYPICAL WELLS. 



67 



Wells in Jordan River and Utah LaJce valleys — Continued. 



Name of owner. 



Location. 



Diame- 
ter. 



N. Morquist I T. 2 S., 

M. Holmes ' T. 2 S., 

H. Chambers do . 

J. Jones do. 

O. G.Nelson i T. 2 S., 

C. G. Johnson do. 

G. L. Rosengren ' do . 

H. M. Pearson do. 

A. Neilson do . 

H. Larsen do . 

L. Jacobson do. 

W. Dugger T. 2 S., 

A. Hansen do. 

E. E. Osbund do. 

H. C. Monten T. 2 S., 

J. F. Proctor T. 2 S., 

W. Rasmanson T. 2 S., 

H. Covert do. 

Clark T.2S., 

J.M. Wood do. 

E. Erickson do. 

Lumston do . 

(b) \ do. 

Gleason do . 

J. Hays I do. 

J. Harper ' T. 2 S., 

J. M.Mantell ! do. 

J. Mackey ' T. 2 S., 

Barker do . 



R. 1 E. 
R. 1 K. 



sec. 29 . 
sec. 30. 



R. 1 E., sec. 31.... 



R. 1 E., sec. 32. 



R. 1 E., sec. 33. 
R. 1 E., sec. 34. 
R. 1 E., sec. 35. 



R. 1 W., sec. 1 



R. 1 W., sec. 2. 



R. 1 W., sec. 3. 



C) 



T. 2 S., R. 1 W., sec. 6.. 

Parker T. 2 S., R. 1 W., sec. 8.. 

School do 

Snider do 

McAllister | T. 2 S., R. 1 W., sec. 9.. 

H. McKay T. 2 S., R. 1 W., sec. 10. 

H. Harker T. 2 S., R. 1 W., sec. 11. 

W. H. Hague j do 

P. Swendsen i do 

B. Williams I do 

G. Bueger T. 2 S., R. 1 W., sec. 12. 

Western Pickling Co...' do 

S. Benson do 

D. Adamson do 

Creamery do 

A. E. Erickson do 

J. C. Cahoon \ T. 2 S., R. 1 W., sec. 13.. 

Mrs. A. J. Plummer do. 

C) 

M. Bishop 

E. B. Tripp 

A. S. White 

R. P. Binghurst 

Jones 



..do 

..do 

2S.,R. 1 W.,sec. 

..do 

..do 

..do 



Inches. 




Depth. 



Height of Yield pw 
water. minute. 



Feet. 

30 

3.5 

2(X) 

22 

40-50 

29-30 

51 

90 

53 

26 

15 

100 

14 

200 

22 

40 

50 

40 

40 

100 

287 

140 

90 

65 

280 

372 

240 

212 

260 

56 

157 

120 

150 

110 

141 

315 

222 

323 

85 

100 
350 
249 
117 
345 
180 

(iO 
9J 

50 



Feet. 

- 26-27 



Gallons. 



25-34 
26 



- 41 

- CO 



-200 



- 26 



+ 

+ 

- 18 
+ 

- 10 

- 25 

- 37 

- 60 

- 50 



Dry in winter. 



09 _ 

180 I + 
b Owner's name unknown. 



- 36 

+ 
4- 
+ 

- 8 

- 30 

- c^h 

- 10 

- 40 

- 12 

- 



(«) 



Dry, 



20-35 

40 

2 

22 

25 



35 



68 



UNDERGROUND WATER IN VALLEYS OF UTAH. 



Wells in Jordan River and Utah LaTce valleys — Continued. 



Name of owner. 



Location. 



Diame- 
ter. 



Depth. 



Height of 
water. 



Yield per 
minute. 



Inches. 



J. Anderson 

School 

W. Diamond 

M. Parker 

M. Hansen 

(a) 

C. Erickson 

E. Bateman 

(a) 

Bingham School 

J. B. Wright 

E. Gardner 

(a) 

Cooper 

W. D. Runsal 

A. L. Cooley 

Olsen 

Cannon Farm 

R. Egbert 

P. T. Rundquist 

M. Pusler 

J. Peterson 

N. L. Gardner 

G.Hunt 

S. M. Wilmore 

N. Nelson 

(a) 

P. Jansen 

P.J. Wolfi 

Olsen 

H. Brown 

W. L. Bateman 

E. Johnson 

C. Peterson 



T. 2 S., R. 1 W., sec. 15 

do 

T. 2 S., R. 1 W., sec. 22 

....do 

do 

T. 2 S., R. 1 W., sec. 23 

T. 2 S., R. 1 W., sec. 24 

T. 2 S., R. 1 W., sec. 25 

....do 

....do 

T. 2S. 

....do 

T. 2S. 

....do 

...-.do 

T. 2 S., R. 1 W., sec. 30 

T. 2 S., R. 1 W., sec. 33 

T. 2 S., R. 1 W., sec. 34 

....do 

....do 

T. 2 S., R. 1 W., sec. 35 

do 

do 

T. 2 S., R. 1 W., sec. 36 

do 

do : 

do 





3 


, R. 1 W. 


sec. 26 


3 








, R. 1 W. 


sec. 27 








3 







T. 2S.,R. 2 W., sec. 11. 
T. 2S., R. 2 W., sec. 27. 
T. 3S.,R. IE., sec. 2... 
T. 3S., R. IE., sec. 5... 
T. 3S.,R. IE., sec. 6... 
do , 



A. Yelter ' T. 3 S., R. 1 E., sec. 7. 



H. P. Hansen.. 
P. Anderson... 

R. Despain 

C. Williams... 

F. Olsen 

P. A. Yastrop. 
J. P. Jenson... 

E. N. Fish 

J. L. Johnson. 
J. W. Smith... 

H. Pearson 

J. Tarry 

N. Brown 

J. R. Stocking. 
A. J. Wilson... 

J. R. Allen 

J. Ennis 

J. Boulter 

F. B. Ladler... 



T. 3S., R. IE., sec. 8.. 

T. 3 S., R. 1 E., sec. 9.. 

T. 3 S., R. 1 E., sec. 11. 

T. 3 S., R. 1 E., sec. 17. 

T'. 3 S., R. 1 E., sec. 18. 

T. 3 S., R. 1 E., sec. 19. 
do 

T. 3 S., R. 1 E., sec. 21. 

T. 3 S., R. 1 E., sec. 22. 

T. 3 S., R. 1 E., sec. 28. 

T. 3 S., R. 1 E., sec. 29. 

do 

.....do 

do 

T. 3 S., R. 1 E., sec. 32. 

do 

do 

T. 3 S., R. 1 E., sec. 33. 

do 

a Owner's name unknown. 



Feet. 

117 

165 

345 

225 

140 

185 

30 

251 

20 

325 

230 

180 

100 

154 

137 

28 

178 

1,000 

52 

80 

217 

127 

309 

21 

225 

190 

50 

30 

174 

150 

38-40 

14-16 

40 

28 

75 

56 

125 

16 

30 

40 



95 
34 
65 
10 
18 
18-20 
16 
42 
70 
24 
41 
22 
66 
Dry In winter. 



Feet. 

- 50 

- 50 
-110 

- 40 

- 90 

- 24 

- 12 

- 16 

- 60 

- 40 

- 20 



33 

20-30 
30 
24 
18 

53 
25 
17 
8 
75 

17 



25 
70 
45-52 



Gallons. 



LIST OF TYPICAL WELLS. 



69 



Wells in Jordan River and Utah Lake valleys — Continued. 



Name of owner. , Location. 


Diame- 
ter. 


Depth. 


Height of Yield per 
water. minute. 


P. Swindsen T. 3 S.. R. 1 W., soc. 1 

E. Densley do 

C. Densley do 

D. Densley, jr do 

J F Palmer T 3 S R 1 W. sec. 2 


Inches. 
2 
3 


Feet. 
323 
2on 


Feet. 

+ 
-40 


Gallons. 
5 


30 
3 412 
3 236 

250 

212 

3 137 

3 1 156 

3 ; 255 

500 

2 50 
l\ 28 

' 30 

3 .127 

28 

15 




-.^>8 
-43 






TT Gardner T 3 S R 1 W sec 3 


-20 
-40 

-45 
-85 
-75 




J. A. Egbert do 

J Goff 1 T. 3 S., R. 1 W., sec. 12 






B. Wellington i T. 3 S., R. 1 W., sec. 13 

\ J Holt T 3S R 1 W. soc. 1.5 










B. W. Osborne T. 3 S., R. 1 W., soc. 23 

W. R. Wellington do 

C Erickson T. 3 S., R. 1 W., sec. 24... 


12-15 
12-15 


-12 

- 4 

-40 




E Atwood do 




R Carlson do 




A. Yoblong T. 3S.,R. 1 W., sec. 25 

J Smith do 




3 

2 
3 
3 
2 


133 

90 

225 

102 

400 

40 

125 

20 

41 

15 




Creamery T. 3 s Ti i W.. spo. 2fi 


+ 12 
-60 




G. H. Donzy 

C. H. Roberts 

I. Langton 

G. Newbold 

G. Sproul 

L. Andrews 

J. Ennis 

H.J.Allen 

W. H. Garfield 

W.Crane 

Alpine 

W. L. Parry 

M. Densley 

J. Stedman 

J. Beveridge 

Lehi Junction 


T. 3S., R. 1 W., sec. 27 




T. 3 S. R. 3 W., sec. 26 




T. 4 S., R. 1 E., sec. 5 


+ 

+ 

-10 

-35 

- 8 


3 


. ..do 




do 


2 




T. 4 S., R. 1 E., sec. 6 




T. 4 S., R. 1 E., sec. 32 






do 






T. 4 S., R. 1 E., sec. 33. 




42 
21 
25-80 
30 
9QJ 




do 






T. 4 S. R. 1 E .,sec. 24 






T. 4 S., R. 1 W., sec. 3.. 








do 


3 


-40 




do 


3 1.30 ! -40 




T. 5 S., R. 1 E., sec. 4 




32 
15-50 


-20 
-10-40 
+ 25 

+ 
+ 

- 8-10 

-22 

+ 

+ 
+ 

+ 

- 8 




T. 5 S., R. 1 E., sec. 5 







I. Anderson. . 


T. 5S.,R. IE., sec. 7 

.:...do 


2 ; 134 
ui 125 




Thomas College 




J. Wanless 


do 


li 

2 
2 


125 

90-100 

193 

90-100 

12 

145 

75 

12 

20 

145 

130 

135 

300 

330 

330 
.300 




G. Jacobs 


do 


12 


Do do 




D. J. Thurman 


do 


55 


H. T. Davis 


T. 5 S., R. 1 E., sec. 8 




G. Gerney 


do 


li 




T. R. Jones do 




B. W. Brown 

J. Gough 

P. Austin 

(«) 
J. Brown 


. .do.. . 




do 






T. 5 S., R. 1 E., sec. 9 


2 
2 

li 
2 
2 

li 
3 




do 

do 


5 


(a) do 

San Pedro, Los Ange- do 

les and Salt Lake 
R. R. 

Do do 

Do do 


4 
23 

35 


Do 1 do 


li 140 





a Owner's name unknown. 



70 



UNDEEGKOUND WATER IN VALLEYS OF UTAH. 



Wells in Jordan River and Utah LaTce valleys — Continued. 



Name of owner. 


Location. 


Diame- 
ter. 


Depth. 


Height of 
water. 


Yield per 
minute. 


W. Hunger 


T. 5 S., R. 1 E., sec. 9 


Inches. 
2 
14 
li 
2 

li 

li 
2 

2 

3 


Feet. 
145 
140 
158 
132 
130 
145 
270 
201 
460 

160 
160 
140 
150 
543 
263 

33 
162 
130 

90 


Feet. 

- 2 

+ 

+ 

- 6 

+ 

+ 
-25 

+ 

+ 

+ 

+ 

- ^ 

- 2 

+ ■ 

+ 

+ 

+ 

+ 


Gallons. 

(?)25 
9 


Rhodes 


do 


Wing 


.do 


Anderson 


do 


20 


Gilchrist 


do 






T. 5 S., R. 1 E., sec. 10 




D. Wagstafi 


T. 5 S., R. 1 E., sec. 14 . . . 




A. L. Thornton 


do 


2 


American Fork, city 


do 




well. 
A. Green 


T. 5 S., R. \ E., sec. 15 




J. B. Greene 


do 


2 
2 
2 
3 

2h 

6 

14 

2 

2 

2 

2 


40 


J. Stewart 


T. 5 S., R. 1 E., sec. 16 






. .do. .. . 


10 


A. K. Thornton 


do 




T. J. Chipman 


do 




J. Peters 


do 




A. Field 


do 


5 


Mrs. K. Fox 


-do 


10 


(a) 
(a) 


do 


10 


do 


15 


(a) 


.do 


90 
147 
150 
350 
132 
150 
143 
' 140 
140 
164 
200 
165 

195 
156 
147 
135 
160 


20 


(a) 


T. 5 S., R. 1 E., sec. 17 




0. Ellington 


do 


1^ 
2 

2 

2 

2 

2 

li 

14 

2 

3 

2 

2 

2 
2 

2 

2 

■2 
2 
2 
2 
2 
2 

2 
3 
3 
3 
li 
2 
2 
2 
2 
2 
nown. 


+ 

+ 
+ 
+ 
+ 
+ 

+ 3 
+30 

+ 3 
+ 10 
+ 
+ 46 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

-33 

+ 18 






do 






do 


20 


D. J. Thurman 


do 


10 


J.Donaldson 


.do .. 


20 


J. Stewart 


do 




P. Jacobs 


do 


5 


J. Woodhouse 


do 




M. Evans 


do 


(?)100 


Rio Grande Western 


do 


50 


Rwy. 
G.Webb 


T. 5 S., R. 1 E., sec. 18 


40 


S. R. Taylor 


do 




W. H. Chipman ... 

Do 


T. 5 S., R. 1 E., sec. 23 


(?)150 


T. 5 S., R. 2 E., sec. 11. 


(?)200 


B. Willis 


T. 5 S., R. 2 E., sec. 18 






do 


30 


(a) 

J. D. Godey 


T. 5 S., R. 2 E., sec. 19 




20 


-do.. . 


290 
150 
200 
40 
100 
264 




S. E. Davis 


do 


80 


W. Howe 


T. 5 S., R. 2 E., sec. 20 


20 


Clarke 


.do . 




Lott 


T 5 S R 2 E sec 21 


60 


(a) 


T. 5 S., R. 2 E., sec. 23. 


10 


. ..do 




A. F. Adams 


do 


280 
280 


15 


American Fork City. . . 
W^ Anderson 


.do 




T. 5S., R. 2E., sec. 25 

T. 5 S., R. 2 E., sec. 29. . . 


10 


W. D. West 


64 
70 
74 
200 
70 


15 


Do .. 


do 




(a) 

Wadley ... .. . 


do 


35-50 


dc 




W. D. West 


do 






a Owner's name unk 





LIST OF TYPICAL WELLS. 



71 



Wells in Jordan River and Utah Lake valleys — Continued. 



Name of owner. 



Location. 



D. M. Smith 

(a) 
(a) 

L. Olsen 

F. Newman 

Do 

Pastures 

P. H. Aldred 

I. Fox 

Salt Lake City (about 
130 wells). 

J. M. Roberts 

(a) 

M.Norman T. 5 S 

I.Cole : T.6S 



T. 5S., R.2E.,sec. 29. 
T. 5 S., R. 2 E., sec. 32. 

....do 

....do 

....do 

T. 5S., R. 2 E., sec. .35. 

....do 

T. 5S., R. 1 W., sec. 1.. 
T. 5 S., R. 1 W., sec. 12. 
....do 



1 W 



13. 



T. 5S., R 

....do 

R. 1 W., sec. 24 
R.2E., sec. 5.. 



J. S. Johnson do 

H. Gammon T. 6 S., R. 2 E., sec. 7.. 

H. Gillies | do 

D. A. Gillis I T. 6S., R. 2 E., sec. 8.. 

J. K. Parcell | T. 6 S., R. 2 E., sec. 10. 

N. Knight j T. 6 S., R. 2 E., sec. 14. 

Colorado Fish Co do 

N.J. Knight do 

W. Knight do 

J. S. Park i T.6S. 



A. N. Holdaway. 
M. Holdway 

B. Larsen 

Wride& Allen... 
G. A. Slumway.. 
J. A. Loveless... 
A. L. Mechum. .. 

D. C. Daniels 

H. C. Scott 

J. H. Clinger 

Creamery 

J. W. Park 

W. G. Williams. . 

S. L. Aldred 

W. Gammon 

P. 11. Cluff 

T. W. Whisble... 

J. A. Johnson 

N. Lydian 

S. McFee 

A. Holliday 

W. Cox 

P. C. Bumrell.... 
Utah Sugar Co.. 

W. L. Camp 

N. A. Nelson 

R. A. Hills 

Provo resort 

G. Baum 

W. D. Roberts... 



T. 6S. 

do 

T. 6S. 

do 

T. 6S. 



R.2E. 
R. 2E. 



sec. 15. 
sec. 17. 



R. 2 E., sec. 18. 



T. 6S. 
do 

T. 6 S. 

do 

do 

T. G S. 
do 

T. OS. 

T. 7 S. 
do 

T. 7S. 

do 

do 

do 

T. 7S. 

do 

do 

do 

T. 7 S. 

T. 7S.; 

T. 7S., 
T 



R. 2E., sec. 21. 
S., R. 2 E., sec. 23. 
S., R. 2 E., sec. 24. 
S., R. 2 E., sec. 26. 

R. 2 E., sec. 28. 



R. 2 E., sec. 34. 



Diame- 
ter. 



Inches. 
2 
2 
2 
2 
2 
2 



2 
2-6 



2-3 
2 
3 
2 
2 





,; 


, R. 2E. 


sec. 35 


2 


, R.3E. 


sec. 31 




, R.2E. 


sec. 1 


o' 

2 
2 
2 
2i 
2 


, R.2E. 


sec. 2 






, R. 2 E. 


sec. 3 . 















,R.2E. 


sec. 4 




, R. 2 E. 




o 


, R. 2E. 


sec. 10 




, R.2E. 


sec. 11 


2 



Depth. 



Feet. 
115 
150 

80 
160 
150 

90 
100 
100 
100 
100 

258 

112 

160 

210 

130 

110 

112 

110 

72 

110 

250 

60 

300 

72 

12C-140 

100 

100 

110 

• 104 

52 

40 

65 

110 



Height of Yield per 
water. I minute. 



Feet. 
+ 20 

+ 



Gallons. 



+ 

+ 7ins. 

+ 30 

+ 

+ 

+ 14 

+ 

+ 

+ 

+ 11 

+ 

-67 

-80 
-40-55 

-62 

+ 1-10 

+ 

+ 12 

+ 

+ 

-50 

-36 

-60 



S., 

a Owner's name unknow 



125 


+ 


110 


+ 


130 


+ 


210 


- 


24 


- 


50 


- 


217 


+ 


145 


+ 


145 


+ 


145 


+ 


150 


+ 


130 


+ 


135 


+ 


110 


+ 


128 


+ 


35 


- 


.50 


- 


342 


+ 


12 


- 


184 


+ 



25 
40-45 



45 



(?)2,000 
32 



(?)260 
(?)100 



(?) 1-200 
30 



(?)100 
2& 



72 UNDERGROUT^D WATER IN VALLEYS OF UTAH. 

Wells in Jordan River and Utah LaJce valleys — Continued. 



Name oi owner. 


Location. 


1 


Height of 
water. 


Yield per 
minute. 


Westron 


T. 7 S., R. 2 E. sec. 11 


Inches. Feet. 
2 180 
li 160 
2 ; 168-178 
2 1 150 

2 170 

3 175 

3 192 

n 248 


Feet. 

+ 
+ 
+ 
+ 
+ 
+ 

+ 35 
+ 12 


Gallons. 


W. B. Johnson 

M. Christensen 

B. Johnson 

W. Carter 


do 


15 


do 


10 


..do 


45 


do 


40 


Rio Grande Western 
Rwy. 

San Pedro, Los Ange- 
les and Salt Lake 
R. R. 

W. R. Pike 


T. 7S., R. 2E., sec. 12 

do 


(?)120 
(?)150 


do 


40 


Do- 


do 


2 


198 
168 
168 
180 
150 


36 


W. J. Woodhead 

H. Manney 

Hospital 

W.Scott 

S. W. Sharp 

Farris Bros 

S.Copp 

WatMns & Taylor 

(a) 

A. B. Johnson 

G. T. Peay 

A. W. Hanrer 


do 


+ 
+ 
+ 

+ 


60 


do 


60 


do 






:....do 


2 
2 


55 


do 


197 i + 
'l85 : + 
175 i + 
300 + 
145 + 


30 


do 


60 


do 


2 


9 


do 


2 


T. 7 S., R. 2 E., sec. 14 


n 


20 


do 


170 
137 






T. 7 S., R. 2 E., sec. 16 


2 

2 

li 

2 

3 

2 

2 

li 

2 

2 

3 

li 

li 

2 

2 

3 

2 

2 

2 

2 


+ 5 


30 


T. 7 S., R. 3 E., sec. 6 


140 +2 
333 +20 


40 


T. E. Thurman 


do 


35 




T. 7 S., R. 3 E., sec. 8 


150 
270 
180 
220 
299 
128 


+20 
+ 

+10 
+ 4 

+ 

+ 


15 


Utah Co. Infirmary... 

H. M. Dougal 

Do 


T. 7S., R. 3E., sec. 17 

T. 7 S., R. 3 E., sec. 29 


70 
40 


T. 7 S., R. 3 E., sec. 30 


20 


Clubhouse 

Do 


do 


5 


do 


10 


P. Boyer 

Rio Grande Western 
Rwy. 

J. B. Stevenson 


T. 7 S., R. 3 E., sec. 31 


150' 1 + 
220 +30 

232 - + 


18 


T. 7 S., R. 3 E., sec. 32 

do 


80 
15 


T. 7S., R. 3 E., sec. 33 


101 
131 
240 
230 
135 
115 
128 
105 
22 


+ 
+ 

+ 
+ 18 

+ 
+ 
+ 

+ 


12 


D. Wheeler 


.do 


25 


D. Clark 


do 




A. Cox .... 


do 


(?)120 


W. Findley 


do 


25 


(a) 

A. Oakley 


do 


70 


.do 


30 


J. McCurdey. . 


do 


30 


do 




(a) 


do 


2 


120 ! + 
245 + 
25 


20 


T. L. Mendenhall 


do 


45 


S. Fuller 


.do 


\ 


M. Dougal 


do 


2 

IJ 

li 

2 

2 

n 


230 
130 
132 
145 
217 
138 
160 
100 


+ 
+ 
+ 
+ 
+ 
+ 


10 


E. P. Brinton . 


do 


20 




do 


10 


Daley 


do 


9 


F. W. Phillips 


....do 


65 


(a) 


do 


30 


W. Brookes 


T. 8 S., R. 1 E., sec. 11 


10 


(a) 


do 


- 4 

+ 




T. 8S.,R. IE., sec. 24 


7 



a Owner's name unknown. 



LIST OF TYPICAL WELLS. 



73 



Wdls in Jordan River and Utah Lake valleys — Continued. 



Name of owner. 



J. D. Evans 

E. L. Oltioon 

IT. Otis 

C. Barney 

(«) 
J. Hall 

J. S. Bellows 

■\V. J. Soloman 

R, Hunter 

J. E. Creer 

P. Poulsen do. 

P. Neilson T. 8 S. 

E. P. Thomas ....' do 

A. Green 1 T. 8 S. 

Do I do 



Location. 



R. 2E. 
R. 2 E. 



sec. -1. 
sec. 4. 



T. 8S. 
T. 8 S. 
....do 
....do 
....do 
....do 
T. 8S. 
T. 8S. 

....do 

....do 

T. 8 S., R. 2 E., sec. 



R. 2E. 
R. 2E. 



sec. I . 
sec. 8. 



R. 2 E., sec. 10. 



R. 2E., sec. 12. 



Creamery 

San Pedro, Los Ange- 
les and Salt Lake 
R.R 



A. T. Money 

R. W. Monej' 

W. R. Simmons 

A. M. Furgeson 

P. E. Nelson 

Irrigation Co 

Lake Shore Canal 

E. M. Robertson 

N. P. Hansen 

(a) 
(a) 

G. McClellan 

Do 

Do 

Do 

N. Thompson 

D. L. Hoff 

E. Ludlow 

C. Howe 

T. Cahoon 

(") 

(") 

O. Christensen 

D. C. Markham 

G. Hales 

(a) 
N. P. Jensen 

B. Isaac 

(«) 
P. Thomas 

F. Malley 

Howe 

G. Howe 

(«) 

Stewart's ranch 

Do 



T. 8S., R. 2E., sec. 13. 



....do 

T. 8S., R. 2E., sec. 14.. 

....do 

T. 8S., R. 2E., sec. 1.5.. 

....do 

....do 

....do 

....do 

T.8S., R. 2E., sec. 16.. 

....do 

T. 8S.,R. 2E., sec. 18.. 

....do 

T.8S., R. 2E., sec. 19.. 

do 

do 

do 

T. 8S.,R. 2E.,sec. 20.. 
T. 8S., R. 2E., sec. 21.. 

do 

do 

do 

T.8S., R. 2E., sec. 22.. 

do 

T. 8S.,R.2E., sec. 23.. 

do 

do 

T. 8S., R. 2E., sec. 2.5.. 
T. 8S., R. 2 E., sec. 26. 

do 

T. 8S., R. 2 E., sec. 27. 

do 

T. 8S., 

do. 

T. 8 S. 

do. 

do. 

do. 



R. 2 E., sec. 28.... 



R. 2 E., sec. 29. 



Diame- 
ter. 



Depth. 



Height of 
water. 



Inches. 



Feet. 
438 
366 
380 
175 
112 
175 
225 
400 
230 
350 
400 
390 
142 
430 
280 
260 
220 

405 
380 

423 I 
374 
380 
400 j 
500 
373 i 
160 I 
380 
450 I 
412 ! 
387 j 

170 ; 

130 i 
45 I 
475 j 
333 
250 
560 
400 
286 

385 
3(i0 
250 
137 
318-320 



425 
385 
415 
450 
175 



Feet. 



Yield yer 
minute. 



Gallons. 



+ 
+ 10 

+ 
4- 
+ 

+ 12 
+ 10 
+ 
+ 
+ 10 



« Owner's name unknown. 



74 



UNDERGEOUI^D WATER IN VALLEYS OF UTAH. 



Weils in Jordan River and Utah Lalce valleys — Continued. 



Name of owner. 



Stewart's ranch 

C. Hickman 

S. P. Lorensen. . 

P. J. Lundale 

J. Howe 

J. J. Hansen 

G. Staley , 

Do 

W. O. Creer 

Creamery 

J. Anderson 

M. C. King 

Do 

(«) 
Sugar factory... 

T. B. Jones 

(a) 

H. A. Harlan 

J. P.Holt 

J. G. Robertson. 

G. LeBaron 

McBeath 

J. Webb 

F. Rouse 

J. E. Gardner... 

(a) 
(a) 
(a) 
(a) 
(a) 
(a) 

S. Douglas 

Do 

Dixon Bros 

P. Windward 

T. E. Daniels 

C. Long 

D. LeBaron 

(«) 
A. Bingham 

Do 

Creamery 

C. Hanks 

A. Burke 

J. Sheen 

O. R. Thomas... 

H. Boyle 

J. Job 

Do 

W. M. Phillippi. . 

(a) 

Rudd estate 

A. Steele 

E. Hawkins 

H. Johnson 



Location. 



R. 2 E.,sec 



R. 2E., 
R. 2E., 



sec. 32. 
sec. 33. 



T. 8S., 

do. 

do. 

T. 8S., 
T. 8S., 

do 

do 

do 

T. 8S., R. 2 E., sec. 35. 
T. 8S., R. 3E., sec. 4.. 
T. 8S., R. 3E., sec. 5.. 
T. 8S., R. 3E., sec. 7.. 

do 

T. 8S., R. 3E., sec. 8.. 

....do 

T. 8S., R. 3E., sec. 21. 
T. 8S., R. 3E., sec. 30. 

....do 

....do 

....do.. 

T. 9 S., R. 1 E., sec. 7.. 

1 E., sec. 12. 

1 E., sec. 13. 

1 E., sec. 32. 

2E., sec. 1.. 



T. 9S., 
T. 9S., 
T. 9S., 
T. 9S., 

do. 

T. 9S., 

do. 

T. 9S., 
.....do. 
do. 



R. 2 E., sec' 2. 



R. 2 E., sec. 3. 



T. 9S., 

do. 

do. 

do. 

T. 9S., 

do. 

T. 9S., 

T. 

T. 



R. 2E., sec. 5. 



R. 2 E., sec. 



R. 2E., sec. 7. 



Diame- r»oT^+T1 Height of Yield per 

tor -L'epUl. WQtor miniito 



Inches. 



., R. 2 E., sec. 10 

., R. 2E., sec. 11 , 



T. 9 S., R. 2E., sec. 29 

T. 9 S., R. 2E., sec. 30 

T. 9S., R. 1 W.,sec. 25 

T. 9S.,R. 1 W., sec. 26 

T. 9 S., R. 1 W., sec. 33 

T. 9S., R. 1 W., sec. 35 

T. 9 S., R. 1 W., sec. 36 

T. 10 S., R. IE., sec. 6 

T. 10 S., R. IE., sec. 17 

T. 10S.,R. 1 W., sec. 2 ! 

a Owner's name unknown. 



Feet. 



172 
163 
175 
200 
380 
185 
380 

20 
144 
145 
170 
154 

30 
123 

22 
140 

30 
100 



247 
180 
290 
155 
200 
200 
160 
375 
228 

50 
130 
300 
140 
116 
160 
217 
438 
196 
275 
225 
175 
296 
279 

20 
90-126 
50- 60 
220 
165 
200 

58 

85 
130 
407 



water. 



Feet. 

+ 
+ 
+ 
+ 
+ 
+ 



+ 
+ 15 



+ 1 
+ 20 

+ 



16i 



125 



80 



LIST OF TYPICAL WELLS. 



75 



Wells in Jordan River and Utah Lake valleys — Continued. 



Name of ownor. 


Location. 


Diame- 
ter. 


Depth. 


Height of 
water. 


Yield per 
minute. 


W. M. Phillippi 

W, C. Albertson 


T. 10 S., R. 1 W., sec. 4 


Inches. 
2 
2 

2 
2 

2 

2 


Feet. 

168 

178 

' 307 

300 

420 

77 

412 

70 

334 

160 

8 

50 
70 
60 
53 
116 
238 
138 


Feet. 
-100 

- 3 

- 4 

- 4 

- 3 

- 20 

- 86 
-222 


Gallons. 


T. 10 S., R. 1 W., sec. 9 




J. Riley 


do 




Do 


do 




Baxter. . 


.do 




P. Okleberry 


T. 10 S., R. 1 W., sec. 11 




(°) 


T. 10 S., R. 1 W., sec. 12 




...do 






Rio Grande Western 
Rwv 


do 






W. Finch 


T. 10 S., R. 1 W., sec. 14 


2 




L. E. Thomas 


T. 10 S., R. 1 W., sec. 15 




Goshen Wells 


do 




u 

2 
2 
2 
2 
2 
2 




Do 


do 






. ..do 




H. L. Cook 


do 




Allen.-. 


T. 10 S., R. 1 W., sec. 21 






T. 10 S., R. 1 W.,sec. 30 




(°) 


T. 10 S., R. 1 W., sec. 33. . 









a Owner's name unknown. 



INDEX 



A. ■ Page. 

Alpine, water supply of 49 

American Fork (town), water supply of, 

source of 49 

wells in 49-50 

American Fork (stream) , description of ... . 6, 49 

discharge and run-off of, table showing. 21 

view of 50 

water from, analysis of 30 

use of 49 

American Smelting and Refining Company, 

well of, record of 46 

wells of, water from, analysis of 32 

Analyses of water from various streams and 

springs 30, 32 

Artesian wells. See Wells, flowing. 

B. 

Battle Creek, description of 6 

drainage of, effect of, on wells ..r 51 

water of, use of 49 

Bear River, description of 6 

Beck's hot spring, water from, analysis of. . 30 

Bed rock, water from 50, 53 

water from, methods of obtaining 37, 40 

Benjamin, underground water conditions at. 54 

Big Cottonwood Creek, description of 7, 45 

discharge and run-off of, table showing. 21,25 

rocks on 9 

water from, analysis of 30 

use of 44, 45 

Big Cottonwood Creek Valley, seepage 

measurements in 28 

Big Hollow Creek, description of 53 

Bingham, mines at, water in 37,40 

rocks near : 10 

water supply of, source of 40 

Bingham Canyon, placer mining in 40 

Bingham Consolidated Company, wells of. . 37 

Bingham Creek, description of 39 

Bingham Junction, smelters at 5 

wells at, water from, analyses of 32 

Bonneville region, Pleistocene history of... 12-13 

Bonneville shore line, description of 12-13 

Bonneville terrace, description of 47 

Boutwell, J. M., on discharge of Ontario 

tunnel 37 

on Park City and Bingham mining dis- 
tricts 8 

on well drilled for oil 41 

Brown, R. E., analyses of water by 30 

Bureau of Soils, Department of Agriculture, 
experiments in reclaiming land 

near Salt Lake City made by 43 

Butterfield Canyon, springs m 40 

tunnels driven for water m 37 

Butterfield Creek, description of 39 

Butterfield tunnel, water in, litigation 

caused by 40 



Page. 



Cambrian fossils, occurrence of 

I Cambrian rocks, occurrence of 9, 

Cameron, F. K., analyses of water by 

Cannon farm, well on 

I Capitol llill, reservoir on 

! Carboniferous rocks, occurrence and char- 
acter of 9, 

City canal, discharge of 

City Creek, description of 

discharge and run-off of, table showing. 

rocks on 

water from, analysis of 

use of 

Clarke, F. W., analysis of water by 

Climate, character of 

Colorado Fish Company, well of, descrip- 
tion of 

Comer, H. C, on general section in vicinity 

of Lehi 

Converse, W. A., analyses of water by 

Cooper, William, well of, water from, anal- 
ysis of 

Cottonwood Canyon, view in 

Cox, A . , well of 

Currant Creek, description of 

reservoir on, failure of 

rocks on 

water from, analysis of 

use of 





10 


10 


11 




30 




41 




45 


10 


11 




24 




7 




19 




8 




30 


44 


,45 


30 


33 


13 


-18 



Dalton and Lark tunnel, description of 

water in, occurrence of 

Dams, subsurface, recovery of underground 

water by 

De Bernard, J. H., analyses of water by 

Dead Mans Falls, Cottonwood Canyon, 

plate showing 

Dearborn laboratories, analyses of water by. 
Decker Lake, ditch at outlet of, discharge of. 

Devonian rocks, occurrence of 8,9, 11 

Doremus, A. F., spring discharge measured 

by 

Drainage, character of 

Drainage area discussed, map showing 

Draper, warm-water lakes near, description 

of 

Dry Cottonwood Creek, description of 

water from, analysis of 

Dry Creek, description of 

Dry Creek Canyon, springs in 

Du Chesne River, source of 



44 

5-7 

6 

47 

7 

30 

6,48 

49 



East Jordan canal, discharge of 

East Tintic Mountains, location and eleva- 
tion of 

structure of 

Eighth South street ditch, discharge of 



77 



78 



INDEX. 



rage. 

Electric power, development of 37, 39 

Emigration Creek, description of 7 

discharge and run-off of, table showing. 19 

valley of, rocks in 9 

syncline developed in 37 

water from, analysis of 30 

use of 44, 45 

Emmons, S. F., on descriptive geology 7 

Evans Spring, water of, use of 53 

Evaporation at Utah Lake 17 

F. 

Fault in Wasatch Mountains, description 

of 8,9,10 

Flowing wells. See Wells, flowing. 

Fort Douglas, water supply of, source of . . 44 

G. 

Gammon, Harry, wells of 35, 51 

Gas, natural, occurrence of 32-33 

Geneva, wells at 51 

Geologic history, discussion of 11-13 

Geology of the region 7-13 

Gilbert, G. K., on Lake Bonneville 7, 11, 13 

on oscillations of lake level between 

Provo and Bonneville horizons. 13 

Girty, G. H., fossils found by 10 

Goshen, springs near 55 

water supply of, source of 55 

well at, water from, analysis of 32 

Goshen Valley, underground water condi- 
tions in 55-56 

Great Salt Lake, elevation of 5 

fluctuations of ■ 25-26 

natural gas near 32 

supply of, sources of 28, 33 

water of, analyses of 33, 34 

Grove Creek, description of 6 

water of, use of 49 

Guffey-Galey well, description of 41 

H. 

Hague, Arnold, on descriptive geology 7 

Heber, rainfall at, table showing 15 

Highlands, descriptive geology of 8-11 

Hobble Creek, description of 6 

Homansville Canyon, water developed in.. . 56 

Hot Springs Lake, outlet of, loss in flow at . 25 

Humidity at Salt Lake City, table showing. 16 

Hydrography of the area 18-26 

I. 

Igneous rocks, occurrence of 8,9,10,11 

Inland Crystal Salt Company, well of 43 

Irrigation by artesian wells 36 

J. 

Jap Pond, water of, character of 40 

Jordan and Salt Lake City canal, head gate 

of, view of 12 

wells sunk to increase supply of 49 

Jordan Narrows, Jordan River and canal 

systems in, discharge of 24 

shore lines on west side of 13 



Page. 

Jordan River, area west of, divisions of 38-39 

discharge of 24-25 

flood plain of, wells sunk in 49 

gate at head of, view showing 24 

lowland area west of, description of 41-43 

sewage discharge into 34 

source and course of 6-7 

tributaries of 7, 18-23 

underground water east of, occurrence 

of 43-48 

underground water west of, occurrence 

of 38-43 

upland area west of, description of 39-41 

water from, analyses of 30 

Jordan River Valley, area of 5 

drainage area of, map showing 6 

ground water in, depth to, map show- 
ing 30 

flowing wells in, area of, map showing.. 38 

location and trend of 5 

seepage in 24-25 

topography and drainage of 5-7 

K. 

Kimball Creek, springs in upper valley of . . 55 

water of, use of ^5 

wells along 56 

King, Clarence, on geology of the region ... 7 

Kingsbury, J. T., analyses of water by 30 

Knight, N. J., wells of, description of 50-51 

L. 

Lake Bonneville, description of 11-13 

location of 5 

shore deposits of 39, 55 

Lake Lahontan, location of 11 

Lake Mountains. See Pelican Hills. 

Lake shore, location of 54 

Lakes, warm water, occurrence of 47 

Lehi, artesian wells at, irrigation from 36 

flowing and nonflowing well near, line 

separating 49 

wells at 48 

flow of, decrease in 36 

water from, analyses of 32 

Lehi and vicinity, underground water con- 
ditions of 48-49 

Liberty Park, wells at and near, flow of — 36,44 

Literature, geologic 7-8 

Little Cottonwood Canyon, glaciers adja- 
cent to, relics of 47 

Little Cottonwood Creek, description of 7, 45 

discharge of 25 

rocks on 9 

water from, analysis of 30 

use of 44 

" Little Cottonwood granite," age of 9 

Long Ridge, springs at base of 55 

structure of 11 

Lower Carboniferous fossils, occurrence of. . 10 

M. 

McDonald, T. F., acknowledgment to 56 

Mapleton Bench, descripton of 53 



INDEX. 



79 



Massachusetts State Board of Health, on 
preservation of water supply 

from contamination 34-35 

Measurement of wells, method of 56-59 

Mercur, rocks near K) 

Mesozoic rocks, occurrence of 10 

Metamorphic rocks, occurrence of 8 

Mill Creek, description of 7,45 

discharge and run-off of, table showing 20,25 

ditch south of, discharge of 25 

rocks on 9 

water of, use of 44 

Mill Creek Valley, seepage measurements in 28 

Morgan, E. R., seepage measurements by.. 28 

Mormon pioneers, irrigation by 5 

Murray, smelters at 5 

well at, record of 46 

well near, decrease in 47 

N. 

Natural gas, occurrence of 32-33 

North J ordan canal, discharge of 24 

O. 

Ogden quartzite, thickness of 8 

Oil, search for 41 

Ontario tunnel, discharge of 37 

Oquirrh Mountains, elevation and extent of. 6 

springs in 40 

structure of 10 

Ordovician rocks, occurrence of 11 

P. • 

Paleozoic rocks, occurrence of 8,9 

Paleozoic section in Wasatch Mountains, 

table showing 8 

Palmyra, location of 54 

Park City, mines of, water in 37 

rainfall at, table showing 14 

Parleys Canyon, reservoir at 45 

Parleys Creek, description of 7,45 

discharge and run-oflf of, table showing 20,25 

rocks on 9 

water from, analysis of 30 

use of 44,45 

i';irsons Chemical Company, analyses of 

water by 32 

Payson, artesian well at, irrigation from 36 

location of 54 

water supply of, source of 54 

Payson Creek, water from, analysis of 30 

Pelican Hills, location and altitude of 6 

structure of 10-11 

Pelican Point, flowing wells near 56 

seep springs near 56 

Permian rocks, occurrence and character of. 9 

Peteeneet Creek, description of 

Pipes, flow from vertical and horizontal, 

diagram illustrating 57 

Placer mining in Bingham Canyon 40 

Pleasant Grove, location and underground 

water conditions of 50-51 

water supply of, source of 49 

Pleistocene fault, occurrence of 5? 



Page. 

Pleistocene rocks, occurrence of 10 

water in, character of 43 

Porous deposits, rainfall absorbed by 39-40 

Pre-Cambrian rocks, occurrence and char- 
acter of 8,9 

Precipitation, tables showing 14-15, 19-22 

Provo, location of 5 

rainfall at, table showing 15 

sewage of, disposal of 34 

temperature at, table showing 15 

vicinity of, underground water con- 
ditions in 51-52 

water supply of, source of 51 

wells at , 32, 52 

Provo horizon, tufa at, occurrence and 

character of 13 

Provo River, discharge and run-off of, table 

showing 22 

drainage area of 6 

source and course of 6 

valley of, below mouth of canyon, view 

of , '. 50 

water from, analysis of 30 

Provo shore line, description of 12-13 

Pumping plants for irrigation, favoral)le 

conditions for 39 

Pyle, F. D. , acknowledgment to 56 

Q- 
Quaternary history of the region 11-13 

R. 

Rainfall, tables showing 14-15. 19-22 

Reclamation Service, levels run by 52 

plans of, for Utah Lake project 39 

" Red Beds," occurrence and character of.. 9 

Red Butte Canyon, rocks in 9 

Red Butte Creek, description of 7 

water from, analysis of 30 

use of 44-45 

Reservoirs, profitable locations for 38 

Richardson, G. B., on natural gas near Salt 

Lake City 32 

Riggs, R. B., analyses of water by 30 

Rio Grande Western Railway, wells of 32, 

42, 44, 48, 52 

Rock Creek Canyon, rocks in 10 

Rose Canyon . springs in 40 

Rudy Well , description of 35. 42, 43 

S. 

Salt Creek, source and course of 6 

Salt Lake City , authorities of, wells sunk by, 

inl890 49 

humidity , mean relative, at 16, 18 

location of 5, 43 

lowland area south of, description of .. 45-47 

natural gas supply of, source of 32-33 

rainfall at 14, 17-18 

rocks in vicinity of 8,9 

sewage of, disposal of 34 

temperature at 15. 16, 18 

thermal springs at. description of 44 

underground water conditions of 43-45 



80 



II^DEX. 



Page. 
Salt Lake City, upland area south of, de- 
scription of 47-48 

water supply of, precaution to avoid 

contamination of 34 

source of 44-45 

wells at 42, 44 

flow of , decrease in 36 

wind velocity at, table showing average. 16 
Salt Lake City Spring, water from, analysis 

of 30 

Salem, location of 54 

underground water conditions in 54 

San Pedro, Los Angeles and Salt Lake Rail- 
road, wells of 48,52,53,54 

Sandy Spring, water from, analysis of 30 

Santaquin, location of 54 

water supply of, source of 54 

Santaquin Creek, description of 6 

water from, analysis of 30 

use of 54 

Sedimentary rocks, occurrence of 8, 9, 11 

Seepage, measurements of 28 

Sewage, disposal of, precautions taken for. 34 

Silurian rocks, occurrence of 8,9, 11 

Slichter, C. S., on measurement of water 

flow from pipes 56 

on method of measurement of wells 56-59 

Smelters, smoke from, injury by 32 

Smith, G. O., and Tower, G. W., on ground 

water in Homansville Canyon. . 56 

on the Tintic district 7 

Smith, J. F., jr., discharge data furnished 

by 24 

Snow, G. W., acknowledgment to 56 

South Jordan canal, description of 39 

discharge of 24 

Spanish Fork (town) , location of 53 

water supply of, source of 53-54 

wells at 53-54 

flow of, decrease in. . . : 36 

Spanish Fork (stream), discharge and run- 
off of, table showing 22 

drainage area of .^ 6 

source and course of - 6 

water from, analysis of 30 

use of ^ 54 

Spring Creek, flow of 46, 52 

Spring Lake, location of .' 54 

water supply of, source of 54 

Springs, occurrence of 40, 44, 47, 50, 55 

water of, character of 31 

Springs, hot, occurrence of 29, 49 

Springville, description of 53 

vicinity of, underground water condi- 
tions in 52-53 

wells at 53 

water from, analysis of 32 

Spurr, J. E., or the Mercur mines 7-8 

Stanbury Island, shore lines on 13 

Streams, water of, character of 30, 31 

Structure of the Highlands 8-ll 

Swendsen, G. L., acknowledgments to 24 

hot springs discovered by '. 49 



T. Page. 

Tanner, Caleb, acknowledgment to 51 

discharge measurement by 25 

Taylorville roller mill, flume at, discharge 

at 25 

Temperature, tables showing 15-16 

Tertiary history of the region 11 

Tertiary rocks, occurrence of 8, 10, 11 

Thistle, rainfall at, table showing 15 

Timpanogas canal, seepage of 28 

Tintic Mountains, springs in 55 

Todd, J. E., on measurement of water flow 

from pipes t 56 

Topography, features of 5-7 

Tower, G. W., and Smith, G. O., on ground 

water in Homansville Canyon. . 56 

on the Tintic district 7 

Traverse Mountains, structure of 8-9, 10 

Tufa, calcareous, occurrence and character 

of 13 

U. 

Underground water. See Water, under- 
ground. 

United States Mining Company, wells of, 

water from, analyses of 32 

United States Weather Bureau, meteoro- 

logic data from records of 13-17 

Utah and Salt Lake canal, description of . . 39 

discharge of 24 

Utah County Infirmary, well at 52 

Utah Experiment Station, experiments in 
.reclaiming land near Salt Lake 

City made by 43 

Utah Lake, description of 6 

elevation of 5 

evaporation at 17 

fluctuations of 23-24 

hot springs at 49 

northern end of, view of 12 

sewage discharge into 34 

streams tributary to 6, 18-23 

supply of, source of 23-24 

underground water west of, occurrence 

of 56 

water from, analyses of 30 

Utah Lake project, plans for 39 

Utah Lake Valley, area of 5 

drainage area of, map showing 6 

flowing wells in, area of, map showing. . 48 
ground water in, depth to, map show- 
ing 30 

location and trend of 5 

topography and drainage of 5-7 

undergrond water in, occurrence of 48-56 

Utah Sugar Company, wells of 48 

wells of, water from, analysis of 32 

Ute limestone, thickness of & 

v.. 

Vegetation, character of 7 

Volcanic rock, outcrop of 8. 



INDEX. 



81 



W. Page. 

Wadley, Williair, & Sons, water developed 

bj ,unneling into bed rock .50 

Walcott, C. D., on Big Cottonwood Cam- 
brian section 7 

Wann Creek, source of 31,55 

water from, analysis of 30 

Wasatch fault, description of 8,9, 10 

Wasatch limestone, occurrence, thickness, 

and dip of 8 

Wasatch Mountains, elevation of 5,6 

geology of 8-9 

Paleozoic section in 8 

rainfall caused by 18 

vegetation on 7 

view of 5 

Water, analyses of 30,32 

contamination of, precaution taken to 

avoid 34 

sanitary character of 34 

Water, underground, depth to, map show- 
ing 30 

distribution of 29-30 

occurrence of 38-56 

quality of 30-35 

recovery of 35-37 

source of 27-28 

Water resources, use of, efficiency in 38 

Weber quartzite, occurrence, thickness, and 

dip of 8 

Weber River, description of 6 

IRR 157—06 6 



Page. 

Well sections, plate showing 28 

Wells, data concerning 56-75 

method of measurement of 56-59 

water from, analyses of 32 

W'ells, flowing, area of, in Jordan stiver Val- 
ley, map showing 38 

area of, in Utah Lake Valley, map 

showing 44 

decrease in, cause of 36 

location and description of 35-36, 

46,50,52,53,54-55 

recovery of water by 36 

water of, use of 36 

yield of, table for determining 58 

Wells, shallow, recovery of water by 36 

Wells, typical, list of 59-75 

West Jordan, well at, water from, analysis 

of 32 

West Mountain, warm spring near 55 

Westfall, J., information furnished by 52 

Westphal, Gus, well record furnished by... 42 
Widtsoe, J. A., on effects of smelter smoke. 32 

Willow Creek, description of 7 

Wilson, H. M., on wind velocity required 

for windmills 36 

Wind velocity at Salt Lake City, table 

showing average 16 

Windmills, wind velocity required for 36 

Y. 
Yeager, H. F., well record furnished by 46 



CLASSIFICATION OF THE PUBLICATIONS OF THE UNITED STATES GEOLOGICAL 

SURVEY. 

[Water-Supply Paper No. 157.] 

The serial publications of the United States Geological Survey consist of (1) Annual 
Reports, (2) Monographs, (3) Professional Papers, (4) Bulletins, (5) Mineral 
Resources, (6) Water-Supply and Irrigation Papers, (7) Topographic Atlas of 
United States — folios and separate sheets thereof, (8) Geologic Atlas of the United 
States — folios thereof. The classes numbered 2, 7, and 8 are sold at cost of publica- 
tion; the others are distributed free. A circular giving complete lists may be had 
on application. 

Most of the above publications may be obtained or consulted in the following 
ways: 

1. A limited number are delivered to the Director of the Survey, from whom they 
may be obtained, free of charge (except classes 2, 7, and 8), on application. 

2. A certain number are delivered to Senators and Representatives in Congress, for 
distribution. 

3. Other copies are deposited with the Superintendent of Documents, Washington, 
D. C, from whom they may be had at prices slightly above cost. 

4. Copies of all Government publications are furnished to the principal public 
libraries in the large cities throughout the United States, where they may be con- 
sulted by those interested. 

The Professional Papers, Bulletins, and Water-Supply Papers treat of a variety of 
subjects, and the total number issued is large. They have therefore been classified 
into the following series: A, Economic geology; B, Descriptive geology; C, System- 
atic geology and paleontology; D, Petrography and mineralogy; E, Chemistry and 
physics; F, Geography; G, Miscellaneous; H, Forestry; I, Irrigation; J, Water stor- 
age; K, Pumping water; L, Quality of water; M, General hydrographic investiga- 
tions; N, Water power; O, Underground waters; P, Hydrographic progress reports. 
This paper is the eighty-sixth in Series B, and the fifty-third in Series O, the compete 
lists of which follow (PP= Professional Paper; B=Bulletin; WS= Water-Supply 
Paper) : 

SERIES B, DESCRIPTIVE GEOLOGY. 

B '2'6. Observations on the junction, between the Eastern sandstone and the Keweenaw series on 

Keweenaw Point, Lake Superior, by R. D. Irving and T. C. Chamberlin. 1885. 124 pp., 

17 pis. (Out of stock.) 
B 33. Notes on geology of northern California, by J. S. Diller. 1886. 23 pp. (Out of stock.) 
B 39. The upper beaches and deltas of Glacial Lake Agassiz, by Warren Upham. 1887. 84 pp., 1 pi. 

(Out of stock.) 
B 40. Changes in river courses in Washington Territory due to glaciation, by Bailey Willis. 1887. 

10 pp., 4 pis. (Out of stock.) 
B 45. The present condition of knowledge of the geology of Texas, by R. T. Hill. 1887. 94 pp. (Out 

of stock.) 
B 53. The geology of Nantucket, by N. S. Shaler. 1889. 55 pp., 10 pis. (Out of stock.) 
B 57. A geological reconnaissance in southwestern Kansas, by Robert Hay, 1890. 49 pp., 2 pis. (Out 

of stock.) 
B 58. The glacial boundary in western Pennsylvania, Ohio, Kentucky, Indiana, and Illinois, by G. F. 

WrJ.,3:ht, with introduction by T. C. Chamberlin. 1890. 112 pp., 8 pis. (Out of stock.) 



II SERIES LIST. 

B 67. The relations of the traps of the Newark system in the New Jersey region, by N. H. Darton. 

1890. 82 pp. (Out of stock.) 
B 104. Glaciation of the Yellowstone Valley north of the Park, by W. H. Weed. 1893. 41 pp., 4 pis. 

(Out of stock.) 
B 108. A geological reconnaissance in central Washington, by I. C. Russell. 1893. 108 pp., 12 pis. 

(Out of stock.) 
B 119. A geological reconnaissance in northwest Wyoming, by G. H. Eldridge. 1894. 72 pp., 4 pis. 

(Out of stock.) 
B 137. The geology of the Fort Riley Military Reservation and vicinity, Kansas, by Robert Hay. 

1896. 35 pp., 8 pis. 
B 144. The moraines of the Missouri Coteau and their attendant deposits, by J. E. Todd. 1896. 71 

pp., 21 pis. 
B 158. The moraines of southeastern South Dakota and their attendant deposits, by J. E. Todd. 

1899. 171 pp., 27 pis. 
B 159. The geology of eastern Berkshire County, Massachusetts, by B. K. Emerson. 1899. 139 pp., 

9 pis. 
B 165. Contributions to the geology of Maine, by H. S. Williams and H. E. Gregory. 1900. 212 pp., 

14 pis. 
WS 70. Geology and water resources of the Patrick and Goshen Hole quadrangles in eastern 

Wyoming and western Nebraska, by G. I. Adams. 1902. 50 pp., 11 pis. 
B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell'. 1902. 192 

pp., 25 pis. 
PP 1. Preliminary report on the Ketchikan mining district, Alaska, with an introductory sketch of 

the geology of southeastern Alaska, by A. H. Brooks. 1902. 120 pp., 2 pis. 
PP 2. Reconnaissance of the northwestern portion of Seward Peninsula, Alaska, by A. J. Collier. 

1902. 70 pp., 11 pis. 
PP 3. Geology and petrography of Crater Lake National Park, by J. S. Diller and H. B. Patton. 

1902. 167 pp., 19 pis. 
PP 10. Reconnaissance from Fort Hamlin to Kotzebue Sound, Alaska, by way of Dall, Kanuti, Allen, 

and Kowak rivers, by W. C. Mendenhall. 1902. 68 pp., 10 pis. 
PP 11. Clays of the United States east of the Mississippi River, by Heinrich Ries. 1903. 298 pp., 9 pis. 
PP 12. Geology of the Globe copper district, Arizona, by F. L. Ransome. 1903. 168 pp., 27 pis. 
PP 13. Drainage modifications in southeastern Ohio and adjacent parts of West Virginia and Ken- 
tucky, by W. G. Tight. 1903. Ill pp., 17 pis. 
B 208. Descriptive geology of Nevada south.of the fortieth parallel and adjacent portions of Cali- 
fornia, by J. E. Spurr. 1903. 229 pp., 8 pis. 
B 209. Geology of Ascutney Mountain, Vermont, by R. A. Daly. 1903. 122 pp., 7 pis. 
WS 78. Preliminary report on artesian basins in southwestern Idaho and southeastern Oregon, by 

I. C. Russell. 1903. 51 pp., 2 pis. 
PP 15. Mineral resources of the Mount Wrangell district, Alaska, by W. C. Mendenhall and F. C. 

Schrader. 1903. 71pp., 10 pis. 
PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred 

and third meridian, by N. H. Darton. 1903. 69 pp., 43 pis. 
B 217. Notes on the geology of southwestern Idaho and southeastern Oregon, by I. C. Russell. 1903. 

83 pp., 18 pis. (Out out stock.) 
B 219. The ore deposits of Tonopah, Nevada (preliminary report), by J. E. Spurr. 1903. 31 pp., 1 pi. 

(Out of stock.) 
PP 20. A reconnaissance in northern Alaska in 1901, by F. C. Schrader. 1904. 139 pp., 16 pis. 
PP 21. The geology and ore deposits of the Bisbee quadrangle, Arizona, by F. L. Ransome. 1904. 

168 pp., 29 pis. 
WS 90. Geology and water resources of part of the lower James River Valley, South Dakota, by J. E. 

Todd and C. M. Hall. 1904. 47 pp., 23 pis. 
PP25. The copper deposits of the Encampment district, Wyoming, by A. C.Spencer. 1904. 107 pp., 2 pis. 
PP 26. Economic resources of northern Black Hills, by J. D. Irving, with chapters by S. F. Emmons 

and T. A. Jaggar, jr. 1904. 222 pp., 20 pis. 
PP 27. Geological reconnaissance across the Bitterroot Range and the Clearwater Mountains in Mon- 
tana and Idaho, by Waldemar Lindgren. 1904. 122 pp., 15 pis. 
PP 31. Preliminary report on the geology of the Arbuckle and Wichita mountains in Indian Terri- 
tory and Oklahoma, by J. A. TafE, with an appendix on reported ore deposits in the Wichita 

Mountains, by H. F. Bain. 1904. 97 pp., 8 pis. 
B 235. A geological reconnaissance across the Cascade Range near the forty-ninth parallel, by G. O. 

Smith and F. C. Calkins. 1904. 103 pp., 4 pis. 
B 236. The Porcupine placer district, Alaska, by C. W. Wright. 1904. 35 pp., 10 pis. 
B 237. Igneous rocks of the High wood Mountains, Montana, by L. V. Pirsson. 1904. 208 pp., 7 pis. 
B 238. Economic geology of the lola quadrangle, Kansas, by G. I. Adams, Erasmus Haworth, and 

W.R.Crane. 1904. 83 pp., 1 pi. 



SERIES LIST. Ill 

PP 32. Geology and underground water resources of the central Great Plains, by N. H. Darton. 1905. 

433 pp., 72 pis. 
WS 110. Contributions to hydrology of eastern I'nited States, 1904; M. G. Fuller, geologist in charge. 

1905. 211 pp., 5 pis. 
B 242. Geology of the Hudson Valley between the Hoosic and the Kinderhook, by T. Nelson Dale. 

1904. 63 pp., 3 pis. 

PP 34. The Delavan lobe of the Lake Michigan glacier of the Wisconsin stage of glaciation and 

as.sociated phenomena, by W. C. Alden. 1904. 106 pp.. 15 pis. 
PP 36. Geology of the Perry Basin in southeastern Maine, by G. O. Smith and David White. 1905. 

107 pp., 6 pis. 
B 243. Cement materials and industry of the United States, by E. C. Eckel. 1905. 395 pp., 15 pis. 
B 246. Zinc and lead deposits of northwestern Illinois, by H. F. Bain. 1904. 56 pp., 5 pis. 
B 247. The Fairhaven gold placers of Seward Peninsula, Alaska, by F. H. Moffit. 1905. 85 pp., 14 pis. 
B 249. Limestones of southwestern Pennsylvania, by F. G. Clapp. 1905. 52 pp., 7 pis. 
B 2.50. The petroleum fields of the Pacific coast of Alaska, with an account of the Bering River coal 

deposit, by G. C. Martin. 1905. 64 pp., 7 pis. 
B 241. The gold placers of the Fortymile, Birch Creek, and Fairbanks regions, Alaska, by L. M. 

Prindle. 1905. 89 pp., 16 pis. 
WS 118. Geology and water resources of a portion of east central Washington, by F. C. Calkins. 1905. 

96 pp., 4 pis. 
B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell. 

1905. 138 pp., 24 pis. 

PP 36. The lead, zinc, and fluorspar deposits of western Kentucky, by E. O. Ulrich and W. S. Tangier 

Smith. 1905. 218 pp., 15 pis. 
PP 38. Economic geology of the Bingham mining district of Utah, by J. M. Boutwell, with a chapter 
on areal geology, by Arthur Keith, and an introduction ongeneral geology, by S. F. Emmons. 
1905. 413 pp., 49 pis. 
PP 41. The geology of the central Copper River region, Alaska, by'W. C. Mendenhall. 1905. 133 pp., 

20 pis. 
B 254. Report of progress in the geological resurvey of the Cripple Creek district, Colorado, by Walde- 

mar Lindgren and F. L. Ransome. 1904. 36 pp. 
B 255. The fluorspar deposits of southern Illinois, by H. Foster Bain. 1905. 75 pp., 6 pis. 
B 256. Mineral resources of the Elders Ridge quadrangle, Pennsylvania, by R. W. Stone. 1905. 

86 pp., 12 pis. 
B 257. Geology and paleontology of the Judith River beds, by T. W. Stanton and J. B. Hatcher, with 

a chapter on fossil plants, by F. H. Knowlton. 1905. 174 pp., 19 pis. 
PP 42. Geology of the Tonopah mining district, Nevada, by J. E. Spurr. 1905. 295 pp., 23 pis. 
WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by 

C. R. Keyes. 1905. 42 pp., 9 pis. 
WS 136. Underground waters of Salt River Valley, Arizona, by W. T. Lee. 1905. 194 pp., 24 pis. 
PP 43. The copper deposits of the Clifton-Morenci district, Arizona, by Waldemar Lindgren. 1905. 

375 pp., 25 pis. 
B 265. Geology of the Boulder district, Colorado, by N. M. Fenneman. 1905. 101 pp., 5 pis. 
B 267. The copper deposits of Mi.ssouri, by H. F. Bain and E. O. Ulrich. 1905. 52 pp., 1 pi. 
PP 44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905. 

394 pp., 34 pis. 
WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis. 
B 270. The configuration of the rock floor of Greater New York, by W. H. Hobbs. 1905. 96 pp., 5 pis. 
B 272. Taconic physiography, by T. N. Dale. 1905. 52 pp., 14 pis. (Out of stock.) 
PP 45. The geography and geology of Alaska, a summary of existing knowledge, by A. H. Brooks. 

with a section ofi climate, by Cleveland Abbe, jr., and a topographic map and description 

thereof, by R. U. Goode. 1906. 327 pp., 34 pis. 
B 273. The drumlins of southeastern Wisconsin (preliminary paper), by W. C. Alden. 1905. 46 pp.. 

9 pis. 
PP 46. Geology and underground water resources of northern Louisiana and southern Arkansas, by 

A. C. Veatch. 1906. 
I'P 49. Geology and mineral resources of part of the Cumberland Gap coal field, Kentucky, by G. H. 

Ashley and L. C. Glenn, in cooperation with the State Geological Department of Kentucky, 

C. J. Norwood, curator. 1906. 239 pp., 40 pis. 
PP 50. The Montana lobe of the Keewatin ice sheet, by F. H. H. Calhoun. 1906. 
B 277. Mineral resources of Kenai Peninsula, Alaska: Gold fields of the Turnagain Arm region, by 

F. H. Motfit, and the coal fields of Kachemak Bay region, by R. W. Stone. 1906, 
WS 154. The geology and water resources of the eastern portion ot the Panhandle of Texas, by C. N. 

Gould. 1906. 64 pp., 15 pis. 
B 278. Geology and coal resources of the Cape Li.sburne region. Alaska, by A. J. Collier. 
B 279. Mineral resources of the Kittanning and Rural Valley quadrangles, Pennsylvania, by Charles 

Butts. 



IV SERIES LIST. 

B 280. The Rampart gold placer region, Alaska, by L. M. Prindle and F. L. Hess. 
B 282. Oil fields of the Texas-Louisiana Gulf coastal plain, by N. M. Fenneman. 

WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson. 
1906. 81 pp., 9 pis. 

SERIES O— UNDERGROUND WATERS. 

WS 4. A reconnaissance in southeastern Washington, by I. C. Russell. 1897. 96 pp., 7 pis. (Out of 

stock.) 
WS 6. Underground waters of southwestern Kansas, by Erasmus Haworth. 1897. 65 pp., 12 pis. 

(Out of stock.) 
WS -7. Seepage waters of northern Utah, by Samuel Fortier. 1897. 50 pp., 3 pis, (Out of stock.) 
WS 12. Underground waters of southeastern Nebraska, by N. H. Darton. 1898. 56 pp., 21 pis. (Out 

of stock.) 
WS 21. Wells of northern Indiana, by Frank Leverett. 1899. 82 pp., 2 pis. (Out of stock.) 
WS 26. Wells of southern Indiana (continuation of No. 21), by Frank Leverett. 1899. 64 pp. (Out 

of stock.) 
WS 30. Water resources of the Lower Peninsula of Michigan, by A. C. Lane. 1899. 97 pp., 7 pis. 

(Out of stock.) 
WS 31. Lower Michigan mineral waters, by A. C. Lane. 1899. 97 pp., 4 pis. (Out of stock.) 
WS 34. Geology and water resources of a portion of southeastern South Dakota, by J. E. Todd. 1900. 

34 pp., 19 pis. 
WS 53. Geology and water resources of Nez Perces County, Idaho, Pt. I, by I. C. Russell. 1901. 86 

pp., 10 pis. (Out of stock.) 
WS 54. Geology and water resources of Nez Perces County, Idaho, Pt. II, by I. C. Russell, 1901 

87-141 pp. (Out of stock.) 
WS 55. Geology and water resources of a portion of Yakima County, Wash., by G. O. Smith. 1901 

68 pp., 7 pis. (Out of stock.) 
WS 57. Preliminary list of deep borings in the United States, Pt. I, by N. H. Darton. 1902. 60 pp 

(Out of stock.) 
WS 59. Development and application of water in southern California, Pt. I, by J. B. Lippincott 

1902. 95 pp., 11 pis. (Out of stock.) 
WS 60. Development and application of water in southern California, Pt. II, by J. B. Lippincott, 

1902. 96-140 pp. (Out of stock.) 
WS 61. Preliminary list of deep borings in the United States, Pt. II, by N. H. Darton. 1902. 67 pp 

(Out of stock.) 
WS 67. The motions of underground waters, by C- S. Slichter. 1902. 106 pp., 8 pis. (Out of stock.) 
B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell. 1902. 192 

pp., 25 pis. 
WS 77. Water resources of Molokai, Hawaiian Islands, by Waldemar Lindgren. 1903. 62 pp., 4 pis. 
WS 78. Preliminary report on artesian basin in southwestern Idaho and southeastern Oregon, by I. C. 

Russell. 1903. 53 pp., 2 pis. 
PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred 

and third meridian, by N. H. Darton. 1903. 69 pp., 43 pis. 
WS 90. Geology and water resources of a part of the lower James River Valley, South Dakota, by 

J. E. Todd and C. M. Hall. 1904. 47 pp., 23 pis. 
WS 101. Underground waters of southern Louisiana, by G. D. Harris, with discussions of their uses for 

water supplies and for rice irrigation, by M. L. Fuller. 1904. 98 pp., 11 pis. 
WS 102. Contributions to the hydrology of eastern United States, 1903, by M. L. Fuller. 1904. 522 pp. 
WS 104. Underground waters of Gila Valley, Arizona, by W. T. Lee. 1904. 71 pp., 5 pis. 
WS 110. Contributions to the hydrology of eastern United States, 1904; M. L. Fuller, geologist in 

charge. 1904. 211 pp., 5 pis. 
PP 32. Geology and underground water resources of the ceiitral Great Plains, by N. H. Darton. 1904. 

433 pp., 72 pis. (Out of stock.) 
WS 111. Preliminary report on underground waters of Washington, by Henry Landes. 1904. 85 pp. 

ipl. 
WS 112. Undertiow tests in the drainage basin of Los Angeles River, by Homer Hamlin. 1904. 

55 pp., 7 pis. 
WS 114. Underground waters of eastern United States; M. L. Fuller, geologist in charge. 1904. 

285 pp., 18 pis. 
WS 118. Geology and water resources of east-central Washington, by F. C. Calkins. 1905. 96 pp., 

4 pis. 
B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell. 

1905. 138 pp., 24 pis. 
WS 120. Bibliographic review and index of papers relating to underground waters published by the 

United States Geological Survey, 1879-1904, by M. L. Fuller. 1905. 128 pp. 
WS 122. Relation of the law to underground waters, by D. W. Johnson. 1905, 55 pp. 



SERIES LIST. V 

WS 123. Geology and underground water conditions of the Jornada del Muerto. New Mexico, by C. R. 
Keyes. 1905. 42 \>\k. y pis. 

\VS 136. Underground waters of the Salt River Valley, by \V. T. Lee. 1905. 194 pp., 24 pis. 

B 2M. Record of deep-well drilling for 1904, by M. L. Fuller, E. F. Lines, and A. C. Veatch. 1905. 
106 pp. 

PP 44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905. 
394 pp., 34 pis. 

WS 137. Development of underground waters in the eastern coastal plain region of southern Caliioniia, 
by W. C. Mendenhall. 1905. 140 pp.. 7 pis. 

WS 13S. Development of underground waters in the central coastal plain region of southern Califor- 
nia, by W. C. Mendenhall. 1905. 1G2 pp., 5 pis. 

WS 139. Development of underground waters in the western coastal plain region of southern Cali- 
fornia, by W. C. Mendenhall. 1905. 105 pp., 7 pis. 

WS 140. Field measurements of the rate of movement of underground waters, by C. S. Slichter. 1905. 
122 pp.. 15 pis. 

WS 141. Observations on the groundwaters of Rio Grande Valley, by C. S. Slichter. 1905. 83 pp., 
5 pis. 

WS 142. Hydrology of San Bernardino Valley, California, by W. C. Mendenhall. 1905. 124 pp.. 13 pis. 

WS 145. Contributions to the hydroR)gy of eastern United States; M. L. Fuller, geologist in charge. 

1905. 220 pp., 6 pis. 

WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis. 

WS 149. Preliminary list of deep borings in the United States, second edition, with additions, by 

N. H. Darton. 1905. 175 pp. 
PP 46. Geology and underground water resources of northern Louisiana and southern Arkansas, by 

A. C. Veatch. 1906. 
WS 153. The underfloAV in Arkansas Valley in western Kansas, by C. S. Slichter. 1906. 
WS 154. The geology and water resources of the eastern portion of the Panhandle of Texas, by C. N. 

Gould. 1906. 64 pp., 15 pis. 
WS 155. Fluctuations of the water level in wells, with special reference to Long Island, New York, 

by A. C. Veatch. 
WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson. 

1906. 81 pp., 9 pis. 

The following papers also relate to this subject: Underground waters of Arkansas Valley in eastern 
Colorado, by G. K. Gilbert, in Seventeenth Annual, Pt. II; Preliminary report on artesian waters of a 
portion of the Dakotas, by N. H. Darton, in Seventeenth Annual, Pt. II: Water resources of Illinois, 
by Frank Leverett, in Seventeenth Annual, Pt. II: Water resources of Indiana and Ohio, by Frank 
Leverett, in Eighteenth Annual, Pt. IV; New developments in well boring and irrigation in eastern 
South Dakota, by N. H. Darton, in Eighteenth Annual. Pt. IV; Rock waters of Ohio, by Edward 
Orton, in Nineteenth Annual, Pt. IV; Artesian well prospects in the Atlantic coastal plain region, by 
N. H. Darton, Bulletin No. 138. 

Corre-sjpondence should be addressed to 

The Director, 

United States Geological Survey, 
April, 1906. Washington, D, C. 

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